Accepted Manuscript

Early Carboniferous adakitic rocks in the area of the Tuwu deposit, eastern

Tianshan, NW China: Slab melting and implications for porphyry copper min-

eralization

Yin-Hong Wang, Chun-Ji Xue, Jia-Jun Liu, Jian-Ping Wang, Jun-Tao Yang,

Fang-Fang Zhang, Ze-Nan Zhao, Yun-Jiang Zhao, Bin Liu

PII: S1367-9120(14)00445-3

DOI: http://dx.doi.org/10.1016/j.jseaes.2014.09.032

Reference: JAES 2113

To appear in: Journal of Asian Earth Sciences

Received Date: 1 April 2014

Revised Date: 23 September 2014

Accepted Date: 23 September 2014

Please cite this article as: Wang, Y-H., Xue, C-J., Liu, J-J., Wang, J-P., Yang, J-T., Zhang, F-F., Zhao, Z-N., Zhao,

Y-J., Liu, B., Early Carboniferous adakitic rocks in the area of the Tuwu deposit, eastern Tianshan, NW China: Slab

melting and implications for porphyry copper mineralization, Journal of Asian Earth Sciences (2014), doi: http://

dx.doi.org/10.1016/j.jseaes.2014.09.032

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Early Carboniferous adakitic rocks in the area of the Tuwu deposit, eastern Tianshan,

NW China: Slab melting and implications for porphyry copper mineralization

Yin-Hong Wang a, *, Chun-Ji Xuea, Jia-Jun Liua, Jian-Ping Wanga, Jun-Tao Yangb, Fang-Fang

Zhanga, Ze-Nan Zhaoa, Yun-Jiang Zhaob, Bin Liua

aState Key Laboratory of Geological Processes and Mineral Resources, China University of

Geosciences, Beijing 100083, China;

bNo. 1 Geological Party, Xinjiang Bureau of Geology and Mineral Exploration, Changji

831100, China

Abstract: Existing geochronological and geochemical data for the Early Carboniferous

magmatic rocks in the eastern Tianshan, Xinjiang, have been interpreted in a variety of theories

regarding petrogenesis and geodynamic setting. The proposed settings include rift, back-arc

basin, passive continental margin, island arc, ridge subduction, and post-collisional

environment. To evaluate these possibilities, we present new SHRIMP zircon U–Pb

geochronology and geochemical data, whole-rock geochemical, Hf isotope, and S isotope data

for tonalitic rocks and ores associated with the Tuwu porphyry copper deposit located in the

center of the late Paleozoic Dananhu–Tousuquan arc, eastern Tianshan. SHRIMP zircon U–Pb

dating indicates that the magmatic activity and thus associated copper mineralization occurred

��������������������������������������������������������������

*Corresponding author at: State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, 29 Xue-Yuan Road, Haidian District Beijing 100083, China. Tel.: +86 10 8232 2346 (office); fax: +86 10 8232 2970 E-mail address: wyh@cugb.edu.cn

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ca.332 Ma. The tonalitic rocks are calc-alkaline granites with A/CNK values ranging from

1.16 to 1.58; are enriched in K, Rb, Sr, and Ba; and are markedly depleted in Nb, Ta, Ti, and

Th. They show geochemical affinities similar to adakites, with high Sr, Al2O3, and Na2O

contents and La/Yb ratios; low Y and Yb contents; and slight positive Eu anomalies. In situ Hf

isotopic analyses of zircons yielded positive initial εHf(t) values ranging from 6.9 to 17.2. The

δ34S values of the ore sulfides range from -3.0‰ to +1.7‰, reflecting a deep sulfur source. Our

results indicate that the paleo-Tianshan oceanic slab was being simultaneously subducted

northward beneath the Dananhu-Tousuquan arc, and southward beneath the Aqishan-Yamansu

arc during the Early Carboniferous. The Tuwu adakitic tonalitic rocks were derived from the

partial melting of the subducted paleo-Tianshan oceanic slab, which was subsequently

hybridized by mantle wedge peridotites. The slab-derived magmas have considerably high

copper contents and are highly oxidized, thus leading to porphyry copper mineralization. Such

Early Carboniferous tonalitic rocks that are widespread in the eastern Tianshan define a

province with high potential for copper mineralization.

Keywords: Eastern Tianshan; Tuwu porphyry Cu deposit; Subduction-related adakite;

Tonalite; SHRIMP zircon U–Pb dating; Hf isotope; S isotope

1. Introduction

The Central Asian Orogenic Belt was formed by the amalgamation of various continental

blocks, arc complexes, and accretionary wedges (Pirajno, 2010; Xiao et al., 2010;

Rojas-Agramonte et al., 2011; Goldfarb et al., 2014; Mao et al., 2014). The eastern part of the

Tianshan in northwestern China is part of the southern margin of the orogenic belt (Fig. 1a), and

it separates the Junggar Basin to the north from the Tu-Ha Basin to the south (Fig. 1b). The

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eastern Tianshan is characterized by widespread Carboniferous to Permian granitoids (Chen et

al., 2005b; Wu et al., 2006a), and lesser Devonian granitoids (Li et al., 2006c; Zhou et al., 2010)

and Triassic granitoids (Li et al., 2002; Zhang et al., 2005; Zhou et al., 2010). These eastern

Tianshan granitoids have attracted much attention because they are often associated with

Cu-Au-Fe-Ag mineralization. However, the petrogenesis and geodynamic setting of the

granitoids are still a matter of debate, with suggested settings such as rift (Qin et al., 2002),

back-arc basin (Xu et al., 2003), passive continental margin (Li et al., 2003), island arc (Rui et

al., 2002; Mao et al., 2005; Zhang et al., 2008), ridge subduction environment (Sun et al., 2010,

2011), or post-collision setting (Wang and Xu, 2006a; Gu et al., 2006; Zhou et al., 2008). Some

studies suggest that the porphyry copper-related granitic intrusions in the eastern Tianshan may

have an adakitic affinity (Wang et al., 2001; Liu et al., 2003; Han et al., 2006; Zhang et al.,

2010). The intrusions are mostly tonalitic, granodiorite, and granodioritic porphyry in

composition (Zhang et al., 2004). However, due to the lack of systematic, high-quality

geochronological and geochemical data, the petrogenesis and geodynamic setting of the

adakitic granitoids are poorly understood. As part of the magmatism research in the eastern

Tianshan, this paper thus provides SHRIMP zircon U–Pb geochronological, whole-rock

geochemical, Hf isotope, and S isotope data for the Tuwu intrusive rocks and ores, and

discusses granitoid petrogenesis, the associated porphyry Cu mineralization, the crust–mantle

interaction process, and eastern Tianshan geodynamic setting.

2. Geological setting and deposit geology

The eastern Tianshan region is one of the important producers of Cu (+/-Ni), Au, Fe, and

Ag in China (Zhai et al., 1999; Mao et al., 2008; Deng et al., 2011). The eastern Tianshan may

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be divided into three major tectonic units, the Dananhu–Tousuquan arc, the

Kangguer–Huangshan ductile shear belt, and the Aqishan–Yamansu arc, which are separated

by the regional-scale Kangguer and Yamansu crustal-scale faults (Fig. 1c). The

Dananhu–Tousuquan arc is situated north of the Kangguer fault, is mainly composed of

Devonian to Carboniferous volcanic and intrusive rocks, and contains several porphyry Cu

deposits of different sizes, including the Tuwu, Yandong, Linglong, and Chihu deposits (Fig.

1c). The base of the Dananhu–Tousuquan arc is represented by basaltic to andesitic volcanic

rocks, with locally overlying Lower Carboniferous carbonates and calcareous mudstones (Mao

et al., 2005). The Kangguer–Huangshan ductile shear belt lies between the Kangguer and

Yamansu faults, an area in which most rocks have undergone greenschist facies metamorphism

and ductile deformation, and where there are a number of orogenic Au deposits (e.g., Kangguer)

and magmatic Cu–Ni sulfide deposits (e.g., Huangshan and Huangshandong). The

Aqishan–Yamansu arc is located between the Yamansu and Aqikuduke faults, mainly

comprises Early Carboniferous basalt, andesite, dacite, and tuff of the Yamansu Formation and

Late Carboniferous rhyolite of the Tugutubulake Formation (Ma et al. 1993). The arc hosts

numerous Fe (-Cu) and Cu-Ag-Pb-Zn skarn deposits (e.g., Yamansu). The structural

architecture of the eastern Tianshan is characterized by a series of E-W-trending regional faults,

including the Dacaotan, Kangguer, Yamansu, and Aqikuduke faults (Qin et al., 2003).

The Tuwu porphyry Cu deposit is located in the middle of the Dananhu-Tousuquan arc and

is about 1–3 km north of the Kangguer fault (Fig. 2a). Tuwu, discovered in 1997, is the largest

deposit in the eastern Tianshan, with total Cu reserves of 2.04 million tonnes (Zhang et al.,

2006). The country rocks in the Tuwu area, have well-developed schistosity, strike

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approximately E–W, and dip to the south at 43°to 63°. They can be divided into three lithologic

sections of the Carboniferous Qieshan Group (Fig. 2b).The stratigraphically lowest section is

composed of volcaniclastics and tuff; the middle section is composed of basalt and andesite,

with intercalated dacite and basaltic andesite; and the upper section is composed of sandstone

and polymictic conglomerate, intercalated with tuff and andesite (Wang et al., 2001). The

overlying rocks of the Jurassic Xishanyao Formation consist chiefly of sandstone, siltite,

mudstone, and conglomerate, and they form an angular unconformity with the strata of the

Qieshan Group (Fig. 2b). Intrusive bodies, mostly tonalite and diorite porphyries (Fig. 2b and

3a), were emplaced into the Early Carboniferous volcanic rocks (Fig. 2b and 4b). The tonalitic

rocks are associated with porphyry-style Cu mineralization and surrounding alteration (Zhang

et al., 2004, 2006; Shen et al., 2012, 2014). Within the eastern Tianshan, 23 mineralized stocks

and plugs have been identified, and the largest of these at Tuwu occupies a surface outcrop of

~0.03 km2, with all other bodies occupying areas of <0.01 km2. The intrusions are mostly

irregular in shape where exposed (Fig. 2b).

The Tuwu porphyry Cu deposit consists of the Tuwu and Eastern Tuwu orebodies (Fig. 2b),

which are situated <200 m apart from one another. The mineralization occurs as thick tabular

bodies, and there is no distinct boundary between orebodies and subeconomic wall rocks. Using

a cut-off grade of 0.20% Cu to outline the orebodies, the Tuwu orebody has a continuous length

of 1400 m, a width ranging from 7.6 to 125m, and an average grade of 0.44% Cu. The Eastern

Tuwu orebody is about 1300 m in length, its width varies from 8.0 to 87.1m, and it has an

average grade of 0.30% Cu (Zhang et al., 2006). The orebodies have a thick lenticular surface

morphology, strike nearly E–W direction, and dip to the south at angles of 61°–67° (Fig. 4). The

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orebodies extend down-dip for more than 600 m (Fig. 4), and the Cu mineralization occurs

predominantly in tonalitic rocks (Liu et al., 2003; Zhang et al., 2004; Han et al., 2006).

Ore styles in the Tuwu porphyry Cu deposit mainly include disseminated (Fig. 5a), vein

(Fig. 5b), veinlet and disseminated (Fig. 5c), and scaly (Fig. 5d). Hydrothermal alteration is

zoned from the center of the tonalitic rocks to the margin with the wall rocks as follows: (1)

quartz-core zone, (2) biotite zone, (3) phyllic zone, (4) chlorite –epidote –albite zone, and (5)

argillite zone (Wang et al., 2001). Ore textures mainly include fine- to medium-grain sulfides or

hypidiomorphic-xenomorphic granular textures (Fig. 5e and f). Chalcopyrite is the main ore

mineral in the Tuwu deposit, with minor bornite, pyrite, molybdenite, chalcocite, digenite, and

magnetite. Gangue minerals are quartz and plagioclase, which are associated with sericite,

chlorite, and biotite (Wang et al., 2001).

3. Samples and analytical techniques

Tonalite samples for this study were collected from the Tuwu ore district (Fig. 2b). The

porphyries were altered to variable degrees by formation of biotite, sericite, and propylitic

assemblages. Thus, to best measure the chemical composition, the least altered samples were

chosen for major element, trace element, SHRIMP zircon U–Pb, and Lu–Hf isotope analyses.

These samples are defined as tonalite based on the IUGS classification, but they are also called

plagiogranite porphyry in the literature (Rui et al., 2002; Zhang et al., 2004, 2006; Shen et al.,

2012). They show porphyritic texture and massive structure, and mainly consist of plagioclase

(30–45%), quartz (10–20%), and biotite (5–10%), with accessory minerals that include zircon

and phosphates (Fig. 3b). Plagioclase is charactered by idiomorphic or hypidiomorphic tabular

texture, showing superficial weak sericite alteration (Fig. 3c). Quartz shows xenomorphic

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granular textures and distinct wavy extinction (Fig. 3d). Biotite was mainly yellow-brown in

color, with a hypidiomorphic–xenomorphic flaky or fragmental texture (Fig. 3d).

Zircons were separated from rock samples using flotation and electromagnetic methods at

the Hebei Regional Geological Survey located in Langfang. Zircons were documented with

transmitted and reflected light micrographs as well as cathodoluminescence (CL) images to

reveal their internal structures. The CL imaging was performed at the electronic probe lab of the

Geological Institute of the Chinese Academy of Geological Sciences (CAGS), under an

operating power of 15 kV and 4 nA. Under the guidance of zircon CL images, the zircons were

analyzed for U–Pb isotopic composition and U, Th, and Pb concentrations using a SHRIMP II

ion microprobe with a spot size of 30 μm at the Beijing Ion Probe Centre of the CAGS. Testing

conditions and processes were after Liu et al. (2006). Common lead correction was performed

using 204Pb, with a single testing error of 1σ and a 206Pb/238U weighted average age error of 2σ.

The zircon U–Pb isotope data are presented in Table 1.

Whole-rock compositions were analyzed at the test center of the Beijing Research Institute

of Uranium Geology. Major element analysis was conducted using a Philips PW2404 XRF

with testing precision greater than 1%. Trace element analysis was performed using a Finnigan

MAT Element I ICP-MS, with RSD (10 min) < 1% and RSD (4h) < 5%. For the testing methods,

refer to Gao et al. (2002). The whole-rock geochemical data are presented in Table 2.

In situ Hf isotope analysis was done on zircon grains using a Neptune MC-ICP-MS and a

NewWave UP213 ultraviolet LA-MC-ICP-MS at the MLR Key Laboratory of Metallogeny and

Assessment. During the analyses, He was used as the carrier gas. Depending on zircon size, the

ablating diameter was set at either 55 or 40 μm. International standard zircon sample GJ1 was

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used as a reference. Details of instrumental conditions and test process were given in Wu et al.

(2006b) and Hou et al. (2007). The weighted average of 176Hf/177Hf of the GJ1 zircon samples

was 0.282015 ± 31 (2SD, n = 10), which is in agreement with the values reported in the literature

(Elhlou et al., 2006; Hou et al., 2007). The initial 176Hf/177Hf ratios and εHf(t) values were

calculated with reference to the chondritic reservoir (CHUR) at the time of zircon growth from

magmas. The decay constant for 176Lu of 1.867×10−11 year-1 (Soderlund et al., 2004), and the

chondritic 176Hf/177Hf ratio of 0.282772 and 176Lu/177Hf ratio of 0.0332 (Blichert-Toft and

Albarède, 1997) were adopted. The depleted mantle model ages (TDM) used for basic rocks

were calculated with reference to the depleted mantle at the present-day 176Hf/177Hf ratio of

0.28325, which is similar to that of the average mid-ocean ridge basalt (MORB) (Nowell et al.,

1998) and 176Lu/177Hf=0.0384 (Griffin et al., 2000). Zircon Hf isotope crustal model ages (TcDM)

were calculated using an average continental crustal 176Lu/177Hf ratio of 0.015 (Griffin et al.,

2002). The zircon Hf isotopic data are presented in Table 3.

The δ34S values for sulfides were determined on SO2 obtained by placing a sulfide–CuO

composite (at weight ratio of 1/7) into a vacuum system heated to 980oC. Sulfur isotopes were

measured using a Finnigan MAT251 mass spectrometer at the test center of the Beijing

Research Institute of Uranium Geology. Isotopic data were reported in permil relative to the

Canyon Diablo Triolite (CDT) standard for sulfur. Total uncertainties were estimated to be

better than ± 0.2‰ for δ34S. The sulfur isotopic data are presented in Table 4.

4. Results

4.1. SHRIMP zircon U–Pb geochronology

Tonalite sample TW702-59 (N 42°06′57″, E 92°36′15″) from the Tuwu porphyry Cu

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deposit was chosen for SHRIMP zircon U–Pb analysis. The analytical data are presented in

Table 1. Zircons from the sample are colorless with no obvious inclusions. They are euhedral

and elongate prismatic, with a length to width ratio from 2:1 to 4:1. In zircon CL images, all

grains exhibit well-developed oscillatory zoning (Fig. 6a). The 238U and 232Th contents of

analyzed zircons are 45–144 ppm and 21–91 ppm, respectively, with Th/U ratios ranging from

0.29 to 0.79. These ratios are higher than those of metamorphic zircons (typically <0.1), but

consistent with those of magmatic zircons (Hoskin and Schaltegger, 2003). Therefore, the

SHRIMP zircon U-Pb dating results are interpreted to provide the age of magma crystallization.

Fifteen spot analyses were carried out on zircon grains of the tonalite sample (TW702-59).

Except for four older discordant data spots (9, 11, 12, and 15), the remaining 11 analyses have

206Pb/238U ages ranging from 320.3 to 348.6 Ma, with a weighted mean of 332.3±5.9Ma

(MSWD = 1.5) (Fig.6b). This is interpreted as the age of tonalite emplacement. In summary, the

SHRIMP zircon U-Pb dating indicates that the tonalitic rocks in Tuwu were emplaced in the

Early Carboniferous.

4.2. Whole-rock geochemistry

Whole-rock geochemical data for the Tuwu tonalite samples are presented in Table 2. The

Tuwu tonalite samples are characterized by a limited range in SiO2 (65.34%–68.21%), and plot

in the granodiorite field on a Na2O+K2O vs. SiO2 diagram (Fig. 7a). All tonalite samples record

Al2O3 contents greater than 15% and high Na2O concentrations (2.98%-4.65%). They have

relatively low K2O contents (1.28%–2.49%), and plot in the field of calc-alkaline granites (Fig.

7b). The A/CNK values of the samples (Al2O3/[CaO+Na2O+K2O], molratio) range from 1.16 to

1.58, which is characteristic of peraluminous granite (Fig. 7c). Most of tonalite samples have

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slightly high Mg# values of 40–42, except for two samples with low values of 36 and 37 (Table

2). The CaO, TFe2O3, and P2O5 contents of the tonalite samples range from 1.67% to 2.53%,

3.35% to 5.05%, and 0.13% to 0.15%, respectively. In the Harker diagrams for selected major

oxides (Fig. 8), CaO, TFe2O3, MgO, MnO, P2O5, and TiO2 contents are linearly correlated with

SiO2 contents.

The samples from the Tuwu deposits have steep heavy rare earth element (HREE) patterns

(Fig. 9a) and display slight positive Eu anomalies (Eu/Eu* = 0.93–1.12). High (La/Yb)N ratios

(8.24–10.87) indicate pronounced LREE/HREE fractionation. These features are observed in

the chondrite-normalized REE distribution pattern (Fig. 9a). The samples show strong

enrichment in large ion lithophile elements (K, Rb, Sr, and Ba) relative to high field strength

elements (Nb, Ta, Ti, and Th), and pronounced positive U and Pb anomalies in primitive

mantle-normalized trace element patterns (Fig. 9b). Tuwu tonalite samples also have low

concentrations of Yb (0.84–1.15ppm) and Y (7.51–9.53 ppm). These characteristics, together

with high Sr contents (261–669ppm) and Sr/Y ratios (35–82), indicate that the samples can be

classified as adakites as defined by Defant and Drummond (1990) (Fig. 10a).

4.3. Zircon Hf isotopes

In situ Hf isotope analyses of zircons from the tonalite sample (TW702-59) are shown in

Fig.6a. The zircon Hf isotopic data and calculated results are given in Table 3, and the Hf

isotopic evolution diagram is shown in Fig. 11. Except for four older data spots (9, 11, 12, and

15), the remaining 11 analyses have variable Hf isotopic compositions, with 176Hf/177Hf ratios

of 0.282798–0.283081, εHf(t) values ranging from +6.9 to +17.2, and corresponding two-stage

Hf isotopic crustal model ages (TCDM) values ranging from 239 to 902Ma.

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4.4. S isotopes

Sulfur isotopic compositions for chalcopyrite and pyrite samples from the Tuwu deposit

are presented in Table 4. The δ34S values of six pyrite samples range from +0.2‰ to +1.7‰,

and the δ34S values of four chalcopyrite samples range from –3.0‰ to +0.4‰. In addition, Rui

et al. (2002) and Han et al. (2006b) also obtained δ34S values for sulfides in Tuwu-Yandong ore

field that ranged from –0.9‰ to +1.3‰. Therefore, sulfur isotopes in the Tuwu porphyry Cu

deposit exhibit a narrow range, with an average δ34S value of 0.2‰, very close to meteoritic

values, suggesting an upper mantle source for the sulfur in the Tuwu deposit.

5. Discussion

5.1. Geochronology

Previous studies of most granites in the eastern Tianshan reported that they were formed

between 386 Ma and 228Ma (Fig. 1c; Table 5), and magmatic activity in this region can be

divided into four stages (Zhou et al., 2010; Wang et al., 2014): Late Devonian (386–369 Ma) (Li

et al., 2006c; Tang et al., 2007; Zhou et al.,2010), Early Carboniferous (349–329 Ma) (Sun et al.,

2012; Wang et al., 2014), Late Carboniferous–Late Permian (322–252 Ma) (Mao et al., 2002;

Wu et al., 2006c;) and Early and Middle Triassic (246–228 Ma) (Li et al., 2006a; Yang et al.,

2011). The Late Devonian granitic intrusions mainly occur on the eastern margin of the Tu-Ha

Basin in the eastern Tianshan. They are represented by Jingerquan, Xianshuiquan, and

Sidingheishan bodies, mainly consisting of biotite granite and granodiorite. The Early

Carboniferous granitic intrusions are widely distributed in the middle and western parts of the

eastern Tianshan. They include the Hongshi, Shiyingtan, Xifengshan, Hongyuntan, Yandong

and Tuwu intrusions, mainly consisting of moyite, syenogranite, granodiorite, dioritic

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porphyrite, and tonalite. The Late Carboniferous–Late Permian granites are mainly distributed

in Kangguer-Huangshan ductile shear belt, and include Bailingshan, Kangguer, Weiquan,

Chihu, Huangshan, Sanchakou, and Shuangchagou, which comprise granite porphyry, rhyolite

porphyry, quartz-syenite porphyry, granodiorite, and tonalite. The Early and Middle Triassic

granites are locally exposed as the Weiya, Donggebi, Baishan, and Tudun bodies, and they are

notably less common than the earlier three stages. There is an overall trend in the magmatic

activity in the area, with more of the older intrusions being emplaced in the east and younger

bodies in the middle and west along the length of the Kangguer ductile shear zone.

The internal structure of the large zircon grains from the Tuwu tonalite shows that they

possess good crystal form, uniform composition, and clear oscillatory zoning, which is typical

of magmatic zircons (Fig. 6a). This suggests that zircons were formed by crystallization in the

magmatic system. Our calculated SHRIMP zircon U–Pb age for the Tuwu tonalite of 332.3±5.9

Ma (MSWD = 1.5) is interpreted to represent the age of Tuwu tonalitic body emplacement and

is consistent with ages for the Tuwu–Yandong porphyry Cu mineralization of ca.340–330 Ma

(Liu et al., 2003; Chen et al., 2005a).

Rui et al. (2002) previously obtained a Re–Os isochron age of 323Ma for molybdenite

from the Tuwu porphyry Cu deposit. Qin et al. (2002) used K–Ar and 39Ar–40Ar methods to

determine the ages for hydrothermal sericite and copper sulfide-bearing quartz from the

Tuwu–Yandong region and obtained age of 341 Ma and 347 Ma, respectively. Zhang et al.

(2004) obtained a Re–Os isochron age of 343 Ma for veinlet-hosted and disseminated

molybdenite from the Yandong area. Zhang et al. (2010) obtained a Re–Os isochron age of 326

Ma for molybdenite from the Yanxi porphyry Cu deposit. In summary, these isotopic age data

13 �

suggest that the mineralization ages for the Tuwu–Yandong porphyry Cu deposits range from

340 Ma to 320 Ma. Therefore, the mineralization at the Tuwu porphyry Cu deposit occurred

simultaneously with intrusion of the tonalitic host rock or slightly later.

5.2. Petrogenesis

The petrochemical signature of magmatic rocks records significant information on magma

source region, magmatic process, and tectonic setting (Pearce et al., 1984; Sylvester, 1998;

Barbarin, 1999); therefore, it is important to have a clear understanding of the petrogenetic

history of the Tuwu tonalitic rocks. Apatite is typically assumed to provide a reliable criterion

to distinguish magma types (e.g. S-, I-type) (Chappell and White, 1992; Wolf and London,

1994; Wu et al., 2003; Li et al., 2006b, 2007). Apatite reaches saturation in metaluminous and

weekly metaluminous magmas and the apatite solubility will reduce with the decrease of

temperature and the increase of SiO2 content, but it remains highly soluble in highly

peraluminous magmas (Wolf and London, 1994). These studies indicate that P2O5 and SiO2 in

I–type and A–type granites are negatively correlated, whereas the P2O5 in S–type granite

increases or remains unchanged with an increase in SiO2 (Li et al., 2007, Wu et al. 2007a;

Cheng and Mao, 2010). The P2O5 content of the Tuwu tonalite ranges from 0.13% to 0.15%,

and decreases with increasing SiO2. The results are consistent with an I-type granite (Fig. 13a).

The Y vs. Rb and Th vs. Rb diagrams (Fig. 13c and d) also show the same trend. The Th- and

Y-rich minerals will not crystallize from a metaluminous I-type granite during early stages of

magmatic differentiation, consequently resulting in high Th and Y abundances and a positive

correlation between Y and Rb, and Th and Rb in differentiated I-type granites (Li et al., 2007;

Zhu et al., 2009b). Based on the above interpretations, we suggest that the Tuwu tonalite is an

14 �

I-type granite.

The term adakite was introduced by Kay (1978) and has been used to describe high-Al

(Al2O3>15%) and Na-rich andesitic to dacitic, extrusive or intrusive rocks with a high Sr

content (>600 ppm), strongly fractionated REE patterns (HREE depleted, LREE enriched),

and positive Sr and Eu anomalies (Defant and Drummond, 1990). Based on the whole rock

geochemical data, the Tuwu tonalitic rocks display an adakitic major and trace element

geochemical affinity. They have high Al2O3 and Na2O contents ranging from 15.53% to

16.83%, and 2.98% to 4.65%, respectively. They also have a high Sr concentration (261–669

ppm), and low Y and Yb concentrations (7.51–9.53 ppm and 0.84–1.15 ppm, respectively).

Therefore, the above data indicate that the Tuwu tonalitic rocks display characteristics similar

to adakites. Furthermore, in (Sr/Y) vs. Y and (LaN/YbN) vs. YbN discrimination diagrams (Fig.

10a and b), the Tuwu tonalitic rocks also plot well within the adakitic field.

Several hypotheses have been suggested for the origin of rocks with geochemical

characteristics similar to those of adakitic rocks. The various processes proposed for the genesis

of adakitic rocks include: (1) partial melting of a subducted oceanic slab (Rapp et al., 1999;

Escuder et al., 2007); (2) partial melting of thickened or delaminated lower crust (Gao et al.,

2004; Hou et al., 2004); (3) assimilation and fractional crystallization processes involving

basaltic magma (Macpherson et al., 2006; Richards and Kerrich, 2007); (4) mixing of felsic and

basaltic magmas (Streck et al., 2007); and (5) partial melting of subducted continental crust

(Wang et al., 2008, 2010). We suggest that the Tuwu adakitic tonalitic rocks were most likely

generated by partial melting of subducted oceanic slab based on both geochemical and isotopic

data. This interpretation is supported by the following lines of evidence:

15 �

(1) The Tuwu tonalitic rocks are geochemically similar to slab-derived adakites. Most

samples may be defined as calc-alkaline granites with relatively low K2O contents

(1.28%–2.49%) (Fig. 7b), similar to slab-derived adakites in the northern Tianshan (Wang et al.,

2007) formed by partial melting of subducted oceanic crust. The Tuwu tonalitic rocks also have

slightly high Mg# values of 40–59, and this characteristic is consistent with those of adakites

derived by partial melting of a subducted slab (Defant and Drummond, 1993). Melts from

basaltic lower crust are characterized by Mg# less than 40 regardless of degree of melting,

whereas those with Mg# greater than 40 can be obtained only with a mantle component (Rapp

and Watson, 1995). Therefore, the slightly high Mg# values indicate that interaction between

subducted oceanic crust and mantle wedge peridotite could have formed the Tuwu adakitic

magmas.

(2) The trace element signatures of the Tuwu tonalitic rocks are compatible with the partial

melting of a subducted oceanic slab. The assimilation and fractional crystallization of parental

basaltic magmas would result in positive correlation between Sr/Y, and particularly Dy/Yb

ratios with increasing SiO2 (Macpherson et al., 2006; Tang et al., 2010), but there are no such

obvious correlations in our data (Fig.13a and b). The data clearly plot along a partial melting

trend in the La/Sm versus La and La/Yb versus La diagrams (Fig. 13c and d), indicating that

partial melting of the source, rather than fractional crystallization, was the dominant process.

Moreover, the Tuwu tonalitic rocks have low Y and Yb concentrations, and a geochemical

affinity to MORB in the Sr/Y versus Y diagram (Fig. 10a), which is consistent with other

ore-forming adakitic rocks from the Tuwu–Yandong porphyry Cu belt (Zhang et al., 2006).

(3) The Tuwu tonalitic rocks have slight positive Eu anomalies (Eu/Eu* = 0.93–1.12) and

16 �

positive zircon εHf(t) values (+6.9 – +17.2), similar to a subducted oceanic slab (Mo et al., 2005;

Zhu et al., 2009a). Additionally, the zircons from all samples show an inhomogeneous Hf

isotopic composition, with variations of as much as 10.3 ε units, indicating interaction between

the subducted crust with less radioactive Hf geogenesis and mantle sources with more

radioactive Hf geogenesis (Bolhar et al., 2008). This is because the zircon Hf isotope system

has a high closure temperature (Patchett, 1983; Cherniak and Watson, 2003), and the isotope

ratio remains unchanged during partial melting or fractional crystallization. This is consistent

with the explanation from various workers regarding Hf isotopic inhomogeneity in zircon

(Griffinet al., 2002; Li et al., 2007; Bolhar et al., 2008). Therefore, the Tuwu tonalitic magmas

likely reflected interaction between a subducted slab and mantle wedge peridotite.

In summary, the hypothesis of partial melting of a subducted oceanic slab is our favored

interpretation for the genesis of the Tuwu tonalitic rocks, although there might have been minor

interaction between slab-derived magmas and mantle wedge peridotite during magma ascent.

Moreover, based on the formation conditions for adakites (Martin, 1999; Rapp et al., 1999;

Defant et al., 2002), we suggest that the Tuwu ore-bearing tonalitic rocks formed during fast

and oblique convergence between the paleo-Tianshan oceanic plate and the

Dananhu-Tousuquan island arc (Defant and Drummond, 1990; Oyarzun et al., 2001).

5.3. Implications for Cu mineralization

Different mineral deposit types are associated with different geodynamic environments,

and thus have distinct distribution in time and space (Meyer and Saager, 1985; Deng et al.,

2013, 2014; Mao et al., 2014; Santosh et al., 2014). With respect to porphyry copper deposits,

the relationship between subduction environments and adakitic rocks is well documented

17 �

(Sillitoe, 1972; Richards and Kerrich, 2007; Hou and Cook, 2009; Shen et al., 2014). Numerous

porphyry and other hydrothermal base and precious metal deposits are shown to be associated

with adakitic rocks in various parts of the world, such as the late Miocene Los Pelambres

porphyry Cu deposit in the Andes (Reich et al., 2003), the Eocene-Oligocene Yulong porphyry

Cu-Mo belt in eastern Tibet (Hou et al., 2003; Cooke et al., 2005), and the mid-Miocene

Gangdese porphyry Cu belt in southern Tibet (Hou and Cook, 2009). The three largest

porphyry Cu deposits in the world, E1 Teniente, Chuquicamata, and Río Blanco–Los Bronces,

are considered by many workers to be related to adakites derived by partial melting of a

subducted oceanic slab (Reich et al., 2003; Jiang et al., 2012).

The adakites derived from partial melting of a subducted slab have been shown to be

fertile for Cu mineralizations (Thiéblemont et al., 1997; Defant et al., 2002; Mungall, 2002), so

that a very favorable tectonic setting for the generation of porphyry Cu deposits is above

subduction zones (Sillitoe, 1972; Defant et al., 2002; Reich et al., 2003; Yang et al., 2012, 2014).

The adakitic magmas derived from slab melting in the Tuwu area were favorable melts for the

generation of porphyry Cu mineralization as evidenced by:

(1) The δ34S values of sulfides from the Tuwu porphyry Cu deposit range from –3.0 to

+1.7 ‰, with an average value of +0.2 ‰, which is very close to that of meteorite, implying that

the sulfur was probably derived from a mantle source. Thus, we suggest that the mantle

probably played an important role in providing water and sulfur to the Tuwu magma.

(2) Slab-derived adakitic magmas, together with the metasomatized mantle wedge,

provide relatively large amounts of chalcophile elements (Cu) and volatiles, such as H2O and

Cl, to a porphyry Cu magmatic-hydrothermal system (McDonough and Sun, 1995; Rudnick

18 �

and Gao, 2003; Ling, et al. 2009; Sun et al. 2010, 2011). Such magmas resulted in the

favorable conditions for porphyry Cu mineralization in the Tuwu area (Liu et al., 2010; Sun et

al., 2010).

(3) As chalcophile elements are mainly hosted in sulfides in the mantle (Fleet et al., 1996;

Ballard et al., 2002; Mungall, 2002), the removal of chalcophile elements from the mantle and

their incorporation into magmas can only occur if sulfides are absent in the melted source rocks.

This requires a high oxygen fugacity, with values of log fO2 >FMQ+2 (FMQ represents

fayalite–magnetite–quartz oxygen buffer; Mungall, 2002). The biotite in the Tuwu tonalitic

rocks is rich in magnesium, with Mg/(Mg + Fe + Mn) values ranging from 0.35 to 0.60, and

abundant hematite and magnetite are observed in the ores (Rui et al., 2002; Zhang et al., 2004,

2006). The mineralized porphyries are cut by numerous quartz-sulfide and chlorite-sulfide

veinlets, and locally by carbonate veinlets with minor amounts of sulfides. Therefore, the

adakitic magmas derived from partial slab melting in the Tuwu area are considered to have had

a high oxygen fugacity that was particularly favorable for porphyry Cu mineralization.

5.4. Geodynamic setting

SHRIMP zircon U–Pb dating and geochemical data obtained in this study and by previous

workers show that widespread granitic intrusions occurred in the eastern Tianshan at ca.

340-320 Ma. Magmatism and mineralization in the Tuwu area occurred in the period at ca. 332

Ma, with the mineralization being coeval with or slightly younger than emplacement of the

Tuwu tonalite.

Studies on Carboniferous andesites and granitoids in northern Xinjiang have revealed that

these rocks display an obvious subduction-related component as evidenced by positive bulk

19 �

εNd(t) and zircon εHf(t) values (Sun et al., 2008; Tang et al., 2010; Su et al., 2012; Wang et al.,

2014). There is also a broad consensus that the northern part of Xinjiang experienced

post-collisional magmatism in the latest Paleozoic (Wang and Xu, 2006b; Zhou et al., 2008;

Chen et al., 2012; Yang et al., 2012). The eastern Tianshan is suggested to have been in a

post-collision extensional setting since Early Permian, as supported by an ophiolite as young as

~310 Ma and widespread bimodal volcanic rocks (Qin et al., 2002, 2003; Su et al., 2012). A few

workers, however, favor subduction until Late Permian and Early Triassic based on the

presence of Permian mafic–ultramafic complexes suggested to have formed in an island arc

setting (Xiao et al., 2004; Ao et al., 2010; Su et al., 2012). In the Rb vs. (Y+Nb), Rb vs. (Ta+Yb),

and Nb vs. Y tectonic discrimination diagrams (Pearce et al., 1984), and Rb–Hf–Ta diagram, all

granitoid samples plot within the oceanic arc field (Figs. 10a, b, and c), indicating that the Tuwu

tonalitic rocks have characteristics of island arc granites that were formed in a

subduction-related setting.

Subduction zones have been considered as very favorable tectonic settings for the

generation of porphyry Cu deposits (Sillitoe, 1972; Defant et al., 2002; Reich et al., 2003).

Previous studies have shown that the simultaneous southward and northward subduction of the

paleo-Tianshan oceanic plate in the Carboniferous formed the Aqishan–Yamansu and the

Dananhu-Tousuquan arcs, respectively (Wang et al., 2006a; Han et al., 2006b; Zhang et al.,

2010). In the Aqishan–Yamansu arc belt, the Fe (-Cu) and Cu-Ag-Pb-Zn skarn deposits are

widely distributed, including Yamansu, Hongyuntan, Bailingshan, and Weiquan. These

deposits formed during emplacement of granitic intrusions, with associated hydrothermal

activity resulting in the replacement of Carboniferous and Neoproterozoic carbonate and calcic

20 �

clastic rocks (Mao et al., 2005). The Aqishan–Yamansu arc belt formed throughout the

Carboniferous (Li et al., 2003) along the northern margin of the Central Tianshan (Mao et al.,

2005). The Carboniferous Dananhu-Tousuquan arc was generated by the northward subduction

of the paleo-Tianshan plate (Xiao et al., 2004; Mao et al., 2005; Chen et al., 2012). During the

Early Carboniferous dual subduction, the Tuwu adakitic magma were generated by partial

melting of the paleo-Tianshan slab and subsequent hybridization of the mantle wedge

peridotites (Fig. 16). Such slab melts initially have high Cu contents and are highly oxidized,

and thus play a crucial role for generating deposits such as the Tuwu porphyry Cu system (Sun

et al., 2011). Given that adakitic rocks can only form at temperatures above 700� and at

depths greater than 70–85 km, regardless of whether subduction occurs at normal dips or

shallower angles (Sajona et al., 1993; Gutscher et al., 2000; Zhu et al., 2009a), the

paleo-Tianshan oceanic slab must have subducted beneath the Dananhu-Tousuquan sub-arc

mantle to depths of at least 70–85 km during the Early Carboniferous. In such an environment,

generation of Cu-rich adakitic magmas is favored. We therefore speculate that the widespread

Carboniferous–Permian magmatic rocks in the eastern Tianshan hold more potential for Cu

mineralization than is presently recognized.

6. Conclusions

(1) SHRIMP zircon U–Pb dating indicates that magmatic events occurred at ca.332 Ma in

the Tuwu area, and the associated Tuwu porphyry Cu deposit formed during the same period.

(2) The Tuwu tonalite is calc-alkaline; enriched in K, Rb, Sr, and Ba; markedly depleted in

Nb, Ta, Ti, and Th; and shows geochemical affinities similar to those of adakites. The Tuwu

tonalitic rocks have positive εHf(t) values ranging from +6.9 to +17.2, and these εHf(t) values are

21 �

inhomogeneous, with variations of as much as 10.3ε units. The geochemical and isotopic data

for the tonalitic rocks indicate that they were probably derived from the partial melting of a

subducted oceanic slab, and subsequently hybridized by peridotite in the mantle wedge.

(3) The Tuwu adakitic rocks and associated porphyry Cu mineralization in the eastern

Tianshan were generated in an arc setting, and they likely resulted from the northward

subduction of the paleo-Tianshan ocean plate beneath the Dananhu-Tousuquan island arc

during the Early Carboniferous.

Acknowledgements

We are very grateful to the Editor-in-Chief Bor-ming Jahn and three anonymous

reviewers for their constructive comments and assistance in improving the manuscript. We

thank Lianhui Dong, Chief Engineer of Xinjiang Bureau of Geology and Mineral Exploration,

for his great support and assistance during our fieldwork. We also thank Prof. Yusheng Zhai

and Prof. Dicheng Zhu of the China University of Geosciences (Beijing) for a helpful scientific

review of an earlier version of the manuscript. This research was financially supported by the

Program of the China Geological Survey (1212011085471 and 1212011220923), by the Key

Program of National Natural Science Foundation of China (41030423), by the Major Basic

Research Program of People’s Republic of China (2014CB440903), by the Specialized

Research Fund for the Doctoral Program of Higher Education of China (20130022110001), and

by the 111 Project under the Ministry of Education and the State Administration of Foreign

Experts Affairs, China (B07011).

22 �

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38 �

Figure Captions:

Fig. 1. (a) Location of the study area in the Central Asia Orogenic Belt (modified from Zhang et al.,

2009). (b) Sketch map showing geologic units of the Tianshan (modified from Chen et al., 2012). (c)

Simplified geological map of the eastern Tianshan (modified from Huang et al., 2013).

Fig. 2. (a) Geological map of the Tuwu–Yandong district (modified from Shen et al., 2012). (b)

Geological sketch map of the Tuwu porphyry Cu deposit (modified from Pan et al., 2013).

Fig. 3. (a) Field photograph of diorite porphyrite and tonalite. (b) Hand specimen of tonalite. (c)

Photomicrographs of tonalitic rock, showing mineral components and alteration, under

crossed-polarized light. (d) Tonalitic rock with porphyritic texture, under crossed-polarized light.

Abbreviations: Bt-biotite; Pl-plagioclase; Ser- sericite; Q-quartz; Kf- K-feldspar.

Fig. 4. Cross section along section Line 7 with orebody (a) and lithologies (b) in the Tuwu porphyry

deposit (modified from Han et al., 2006).

Fig. 5. Mineralization in the Tuwu porphyry deposit. (a) Disseminated chalcopyrite with

xenomorphic granular texture. (b) Chalcopyrite veins. (c) Pyrite with enterolithic structure. (d)

Scaly molybdenite. (e) Chalcopyrite replacing early pyrite. (f) Chalcopyrite. Photomicrographs are

taken under reflected light (a, b, c, d, e, f). Abbreviations: Ccp-Chalcopyrite; Py-Pyrite;

Mo-Molybdenite.

39 �

Fig. 6. Cathodoluminescence(CL) image of representative zircons (a) and Concordia diagram (b)

for zircons from the Tuwu granites.

Fig. 7. Classification and series diagrams of the Tuwu granites. (a) Na2O+K2O vs. SiO2 plot diagram

(Rickwood, 1989).(b) K2O vs. SiO2diagram (Rollinson, 1993). (c) A/NK vs. A/CNK plot diagram

(Maniar and Piccoli, 1989).

Fig. 8. Harker diagram of granites in the Tuwu porphyry Cu deposit.

Fig. 9. (a) Chondrite-normalized REE and (b) primitive mantle-normalized trace element abundance

spider diagram for the Tuwu granites (normalized data are from Boynton, 1984, and Sun and

McDonough, 1989).

Fig. 10�Plots of (a) Sr/Y vs.Y and (b) (La/Yb)N vs. YbN for the Tuwu granites (modified after Defant

and Drummond, 1990). Data sources: Li et al., 2002; Han et al., 2006; Zhang et al., 2004, 2006.

Fig. 11. (a) εHf(t) vs. U-Pb age diagram. (b) Histograms of zircon εHf(t) values. (c) Histograms of

zircon Hf-isotope crust model age (TCDM).

Fig. 12. Histogram of sulfur isotope composition of sulfides from the Tuwu porphyry copper deposit.

Fig. 13. Diagrams for granitoid classification for samples from the Tuwu granites. (a) P2O5 vs. SiO2

diagram. (b) Na2O vs. K2O diagram. (c) Th vs. Rb diagram (Li et al., 2007). (d) Y vs. Rb diagram (Li

40 �

et al., 2007).

Fig. 14. Dy/Yb vs. SiO2, Sr/Y vs. SiO2, La/Sm vs. La and La/Yb vs. La diagrams for the Tuwu

granites. Data sources: Li et al., 2002; Han et al., 2006; Zhang et al., 2004, 2006.

Fig. 15. Tectonic discrimination diagrams for the Tuwu granites. (a) Rb vs. (Y+Nb) diagram (Pearce

et al., 1984). (b) Rb vs. (Yb+Ta) diagram (Pearce et al., 1984). (c) Nb vs. Y diagram (Pearce et al.,

1984). (d) Rb/30-Hf-3×Ta diagram (Harris et al., 1986). WPG, within-plate granites; VAG, volcanic

arc granites; Syn-COLG, syn-collision granites; Post-COLG, post-collision granites; ORG, ocean

ridge granites. Data sources: Li et al., 2002; Han et al., 2006; Zhang et al., 2004, 2006.

Fig. 16. Schematic showing the geodynamic setting of the Tuwu porphyry Cu deposit in the eastern

Tianshan.

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LOI = loss on ignition; A/NK = molecular Al2O3 / (Na2O + K2O); A/CNK = molecular Al2O3 / (CaO + Na2O + K2O); Mg# = 100×molar Mg2+/ (Mg2+ +

Fe2+), calculated by assuming TFeO = 0.9 × TFe2O3; Data sources: a-this study, b-Zhang et al., (2004), c-Li et al., (2002)

�

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Table 5. Summary of geochronological data for granitoids in the eastern Tianshan.

44 �

Locations Dated rocks Dating method Ages/Ma Data sources

Shiyingtan Moyite LA-ICP-MS zircon U-Pb 342±11 Zhou et al. (2010)

Hongshi Syenogranite SHRIMP zircon U-Pb 344±4 Sun et al. (2012)

Kangguer Rhyolite porphyry Rb-Sr isochron 300±13 Zhang et al. (2002)

Quartz-syenite porphyry Rb-Sr isochron 282±16 Zhang et al. (2002)

Hongyuntan Granodiorite LA-ICP-MS zircon U-Pb 328.5±9.3 Wu et al. (2006a)

Bailingshan Granodiorite LA-ICP-MS zircon U-Pb 317.7±3.7 Zhou et al. (2010)

Weiquan Granodiorite 39Ar-40Ar 276±2.8 Mao et al. (2002a)

Granodiorite SHRIMP zircon U-Pb 297±3 Wang et al. (2005)

Xifengshan Moyite LA-ICP-MS zircon U-Pb 349±3.4 Zhou et al. (2010)

Yandong Dioritic porphyrite SIMS zircon U-Pb 340±3 Shen et al. (2014)

Tonalite SIMS zircon U-Pb 332.2±2.3 Shen et al. (2014)

Tonalite SHRIMP zircon U-Pb 335±3.7 Wang et al. (2014)

Tonalite SHRIMP zircon U-Pb 333±4 Chen et al. (2005a)

Tuwu Tonalite SHRIMP zircon U-Pb 332.3±5.9 This study

Tonalite SHRIMP zircon U-Pb 334±3 Chen et al. (2005a)

Tonalite SHRIMP zircon U-Pb 333±2 Liu et al. (2003)

Chihu Tonalite SHRIMP zircon U-Pb 322±10 Wu et al. (2006c)

Donggebi Fine-grained granite SHRIMP zircon U-Pb 227.6±1.3 Yang et al. (2011)

Weiya Quartz-syenite SHRIMP zircon U-Pb 246±6 Zhang et al. (2005)

Dioritic porphyrite SHRIMP zircon U-Pb 233±8 Zhang et al. (2005)

Fine-grained granite SHRIMP zircon U-Pb 237±8 Zhang et al. (2005)

Tudun Moyite LA-ICP-MS zircon U-Pb 246.2±2.6 Zhou et al. (2010)

Huangshan Moyite LA-ICP-MS zircon U-Pb 288±17 Zhou et al. (2010)

Sanchakou Tonalite SHRIMP zircon U-Pb 278±4 Li et al. (2004)

Shuangchagou Granodiorite LA-ICP-MS zircon U-Pb 252.4±2.9 Zhou et al. (2010)

Jingerquan Granite LA-ICP-MS zircon U-Pb 376.9±3.1 Zhou et al. (2010)

Xianshuiquan Granodiorite SHRIMP zircon U-Pb 369.5±5.6 Tang et al. (2007)

Sidingheishan Biotite granite SHRIMP zircon U-Pb 386±5 Li et al. (2006c)

Baishan Biotite granite SHRIMP zircon U-Pb 239±8 Li et al. (2006a)

1 Tab

le3

Hf i

soto

pic

data

for z

ircon

s fro

m th

e Tu

wu

gran

ites i

n th

e ea

ster

n Ti

ansh

ana)

Spot

A

ge//M

a 17

6 Yb/

177 H

f 17

6 Hf/17

7 Hf

± 2σ

17

6 Lu/17

7 Hf

176 H

f/177 H

f(t)

176 H

f/177 H

f

CH

UR

(T)

ε Hf(0

) ε H

f(t)

T DM

/Ma

T DM

C/M

a f L

u/H

f

TW70

2-59

, Ton

aliti

c ro

ck, 3

32.3

5.9

Ma

(11

spot

s, w

ithou

t spo

ts 9,

11,

12,

and

15)

, εH

f(t)=

6.9

~ 17

.2

TW70

2-59

-1

321.

3

0.11

4568

0.

2829

50

0.00

0017

0.

0020

15

0.28

2938

0.

2825

72

6.3

12

.9

440

50

6

-0.9

4

TW70

2-59

-2

340.

0

0.18

2536

0.

2830

62

0.00

0032

0.

0029

69

0.28

3043

0.

2825

61

10.3

17

.1

283

25

4

-0.9

1

TW70

2-59

-3

335.

3

0.12

9431

0.

2829

76

0.00

0024

0.

0023

14

0.28

2962

0.

2825

64

7.2

14

.1

404

44

2

-0.9

3

TW70

2-59

-4

323.

6

0.13

3702

0.

2829

24

0.00

0026

0.

0022

31

0.28

2911

0.

2825

71

5.4

12

.0

480

56

5

-0.9

3

TW70

2-59

-5

348.

6

0.15

8374

0.

2829

78

0.00

0024

0.

0033

86

0.28

2956

0.

2825

55

7.3

14

.2

414

44

7

-0.9

0

TW70

2-59

-6

333.

1

0.21

9734

0.

2830

73

0.00

0029

0.

0033

29

0.28

3052

0.

2825

65

10.6

17

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270

23

9

-0.9

0

TW70

2-59

-7

331.

3

0.16

8966

0.

2830

04

0.00

0026

0.

0028

21

0.28

2987

0.

2825

66

8.2

14

.9

369

38

8

-0.9

2

TW70

2-59

-8

320.

3

0.23

4525

0.

2830

32

0.00

0027

0.

0055

92

0.28

2999

0.

2825

73

9.2

15

.1

354

36

8

-0.8

3

TW70

2-59

-9

352.

7

0.20

9396

0.

2830

81

0.00

0025

0.

0049

80

0.28

3048

0.

2825

53

10.9

17

.5

270

23

5

-0.8

5

TW70

2-59

-10

339.

0

0.20

3264

0.

2830

24

0.00

0029

0.

0048

39

0.28

2993

0.

2825

61

8.9

15

.3

359

36

8

-0.8

5

TW70

2-59

-11

354.

8

0.20

0718

0.

2828

77

0.00

0030

0.

0048

54

0.28

2844

0.

2825

51

3.7

10

.4

593

69

6

-0.8

5

TW70

2-59

-12

350.

3

0.18

4403

0.

2829

57

0.00

0024

0.

0032

07

0.28

2936

0.

2825

54

6.5

13

.5

444

49

1

-0.9

0

TW70

2-59

-13

335.

2 0.

2783

84

0.28

2798

0.

0001

54

0.00

6290

0.

2827

59

0.28

2564

0.

9

6.9

74

8

902

-0

.81

TW70

2-59

-14

333.

2 0.

1590

34

0.28

2950

0.

0000

32

0.00

3210

0.

2829

30

0.28

2565

6.

3

12.9

45

5

516

-0

.90

TW70

2-59

-15

353.

8 0.

2313

09

0.28

2867

0.

0000

40

0.00

5216

0.

2828

32

0.28

2552

3.

4

9.9

61

5

724

-0

.84

a)ε H

f(t) =

100

00( {

[ (17

6 Hf /

177 H

f) S -

(176 Lu

/ 17

7 H f)

S(e

λt -

1) ]

/ [ (

176 H

f / 17

7 Hf) C

HU

R, 0

- (17

6 Lu /

177 H

f) CH

UR

( (eλt

- 1) ]

- 1

}. T

DM

= 1

/ λ

ln{1

+ [

(176 H

f / 17

7 Hf) S

- (17

6 Hf /

177 H

f) DM

] /

[(17

6 Hf /

177 H

f) S -

(176 H

f / 17

7 Hf) D

M] }

. TD

MC=

T DM

- ( T

DM

- t )

[ ( f c

c- f s)

/ ( f

cc- f

DM

) ]. f

Lu/H

f = (17

6 Lu /

177 H

f) S /

(176 Lu

/ 17

7 Hf) C

HU

R –

1, w

here

, λ =

1.8

67×1

0-11 /

a (S

oder

lund

et a

l., 2

004)

; (17

6 Lu /

177 H

f) S a

nd (17

6 Hf /

177 H

f) S a

re th

e m

easu

red

valu

es o

f the

sam

ples

; (17

6 Lu /

177 H

f) CH

UR =

0.0

332

and

(176 H

f / 17

7 Hf) C

HU

R, 0

= 0

.282

772

(Blic

hert-

Toft

and

Alb

arde

199

7 );

(176 Lu

/ 17

7 Hf) D

M =

0.03

84 a

nd (17

6 Hf /

177 H

f) DM

=0.

2832

5 (G

riffin

et a

l., 2

000)

; (17

6 Lu /

177 H

f)m

ean

crus

t = 0

.015

; fcc

= [ (

176 Lu

/ 17

7 Hf)

mea

n cr

ust /

(176 Lu

/ 17

7 Hf) C

HU

R]

– 1;

f s =

f Lu/

Hf; f D

M =

[ (17

6 Lu /

177 H

f) DM

/ (17

6 Lu /

177 H

f) CH

UR] –

1; t

= c

ryst

alliz

atio

n tim

e of

zirc

on.

Tab

le

1 T

able

4

Sulfu

r iso

topi

c da

ta o

f the

Tuw

u po

rphy

ry C

u de

posi

t in

the

east

ern

Tian

shan

Sam

ple

no.

Min

eral

s δ34

S‰

TW-9

Py

rite

1.7

TW-1

0 Py

rite

0.8

TW-1

1 Py

rite

0.2

TW-0

05-5

22-5

C

halc

opyr

ite

0.3

TW-0

05-5

22-5

Py

rite

1.6

TW-0

05-5

10-8

C

halc

opyr

ite

0.4

TW-1

5 C

halc

opyr

ite

-1.9

TW-1

6 Py

rite

1.0

TW-1

4 Py

rite

0.4

TW-1

2 C

halc

opyr

ite

-3.0

Tab

le

Figure

1

Figure

1

Fig. 3. (a) Field photograph of diorite porphyrite and tonalite. (b) Hand specimen of tonalite. (c) Photomicrographs of tonalitic rock, showing mineral components and alteration, under crossed-polarized light. (d) Tonalitic rock with porphyritic texture, under crossed-polarized light. Abbreviations: Bt-biotite; Pl-plagioclase; Ser- sericite; Q-quartz; Kf- K-feldspar.

Figure

1

Figure

1

Fig. 5. Mineralization in the Tuwu porphyry deposit. (a) Disseminated chalcopyrite with xenomorphic granular texture. (b) Chalcopyrite veins. (c) Pyrite with enterolithic structure. (d) Scaly molybdenite. (e) Chalcopyrite replacing early pyrite. (f) Chalcopyrite. Photomicrographs are taken under reflected light (a, b, c, d, e, f). Abbreviations: Ccp-Chalcopyrite; Py-Pyrite; Mo-Molybdenite.

Figure

1

Fig. 6. Cathodoluminescence (CL) image of representative zircons (a) and Concordia diagram (b) for zircons from the Tuwu granites.

Figure

1

Figure

1

Fig. 8. Harker diagram of granites in the Tuwu porphyry Cu deposit.

Figure

1

Figure

1

Figure

Fig. 11. (a) εHf(t) vs. U-Pb age diagram. (b) Histograms of zircon εHf(t) values. (c) Histograms of zircon Hf-isotope crust model age (TC

DM).

Figure

Fig. 12. Histogram of sulfur isotope composition of sulfides from the Tuwu porphyry copper deposit.

Figure

Figure

Figure

Figure

Fig. 16. Schematic showing the geodynamic setting of the Tuwu porphyry Cu deposit in the eastern Tianshan.

Figure

45 �

Highlights:

1) Zircon U–Pb dating data indicate that the magmatic events might have occurred around 332 Ma in

the Tuwu region, and the Cu mineralization occurred during the same period as that of the magmatic

rocks formation in the region or slightly later.

2) All the Tuwu tonalitic rocks are calc-alkaline or high–k calc–alkaline, enriched in K, Rb, Sr, and

Ba, makedly depleted in Nb, Ta, Ti, and Th, and show geochemical affinities similar to those of

adakites.

3) The adakitic tonalitic rocks geochemical and isotopic data indicate that they were probably derived

from the partial melting of a subducted oceanic slab, and subsequently hybridized by peridotite in the

mantle wedge.

4) The Tuwu adakitic tonalitic rocks and associated Cu mineralization were generated in an arc

setting, and resulted likely from the northward subduction of the paleo-Tianshan ocean crust beneath

the Dananhu-Tousuquan island arc belt during the Early Carboniferous.