Journal of Asian Earth Sciences 165 (2018) 270–284
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Journal of Asian Earth Sciences
journal homepage: www.elsevier.com/locate/jseaes
Geology, Re-Os and U-Pb geochronology and sulfur isotope of the the T
Donggebi porphyry Mo deposit, Xinjiang, NW China, Central Asian Orogenic
Belt
Chunming Hana,b,⁎, Wenjiao Xiaoa,b, Benxun Sua, Patrick Asamoah Sakyic, Songjian Aoa,
Jien Zhanga, Zhiyong Zhanga, Bo Wana,b, Dongfang Songa, Zhongmei Wanga, Na Zhaoa
a Key Laboratory of Mineral Resource, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China
b CAS Center for Excellence in Tibetan Plateau Earth Sciences, Beijing 100101, China
cDepartment of Earth Science, University of Ghana, P.O. Box LG 58, Legon-Accra, Ghana
A R T I C L E I N F O A B S T R A C T
Keywords: The the Donggebi porphyry Mo deposit in the eastern section of the Eastern Tianshan Orogenic Belt in the
Re-Os Central Asian Orogenic Belt contains Mo metal reserves of 0.5Mt. The deposit is hosted in Early Carboniferous
U-Pb metasedimentary rocks, namely; metasandstone, meta-sandy mudstone . Multiple hydrothermal activities have
The Donggebi porphyry Mo deposit resulted in propylitic, phyllic, and argillic alteration in this deposit. Four stages (I-IV) of hydrothermal activity
Eastern Tianshan Orogenic Belt are identified. Stage I is represented by a mineral assemblage of K-feldspar, quartz and wolframite. Stage II
Central Asian Orogenic Belt
consists of quartz+magnetite+pyrite ± chalcopyrite veinlets/veins with phyllic halos. Stage III consists of
quartz+molybdenite+ pyrite ± galena ± sphalerite ± chalcopyrite veins that are commonly related to
phyllic alteration in the altered rocks. Stage IV has an assemblage of calcite+ gypsum. Molybdenite mainly
occurs in Stages III. Re-Os dating results for molybdenite samples from these two stages yielded an isochron age
of 234.2 ± 1.6Ma (2σ, MSWD=0.25, n=8). Porphyritic granites have a SIMS U-Pb zircon age of ∼236Ma
and it was probably related to the Triassic felsic magmatism in this area. Values of δ34S of sulfides range from
1.5‰ to 3.8‰, with an average value of 2.81 ± 2.24‰ (n=22), reflecting a deep sulfur source. Most mo-
lybdenite samples have high δ34S values (≥3.36‰) relative to other sulfide minerals (i.e., pyrite and chalco-
pyrite) of Stages I to III (δ34S= 1.5–3.8‰, n=18). Based on the geological history and spatial-temporal dis-
tribution of the granitoids, it is proposed that the Mo deposits in the eastern part of the East Tianshan Orogenic
Belt formed in a post-collision extensional setting in the Early Mesozoic.
1. Introduction Cu, Ni, Fe, Au, Ag, Mo,W, Pb and Zn ore deposits, ranging in age from
Neoproterozoic to Cretaceous (e.g., Zhang et al., 1999; Xiao et al.,
The the Donggebi porphyry Mo deposit is located in the eastern 2003a,b, 2009; Berzina et al., 2005; Han et al., 2006; Shen et al., 2012;
section of the Eastern Tianshan Orogenic Belt of northwest China Goldfarb et al., 2013; Seltmann et al., 2014;Chen et al., 2017; Wu et al.,
(Fig. 1). The Eastern Tianshan Orogenic Belt is considered to be the 2017a,b).
southernmost segment of the Central Asian Orogenic Belt (Xiao et al., The Eastern Tianshan metallogenic domain in northwestern China
2004a,b, 2009), which is also known as the Altaid tectonic collage forms a significant part of the Central Asian Orogenic Belt, one of the
(Şengör et al., 1993). The Central Asian Orogenic Belt was formed giant metallogenic belts in the world (e.g., Xiao et al., 2004a,b; Han
mainly as a result of progressive subduction of the Paleo-Asian Ocean et al., 2006; Shen et al., 2012; Seltmann et al., 2014; Chen et al.,
and amalgamation of various arcs and terranes during the Paleozoic 2017;Wu et al., 2017a,b). The Central Asian Orogenic Belt bears one of
(e.g., Şengör et al., 1993; Xiao et al., 2003a,b; Windley et al., 2007). It is the most important porphyry Cu ± Au ± Mo metallogenic provinces
characterized by extensive juvenile crustal growth from the Phaner- in the world (Seltmann and Porter, 2005; Gao et al., 2018; Fig. 1).
ozoic to Mesozoic (e.g., Jahn et al., 2000; Wu et al., 2000, 2002; Located on the northern margin of the Tarim Craton, the Chinese East
Kovalenko et al., 2004). The Central Asian orogenic belt is also one of Tianshan is the easternmost segment of the Tianshan Mountain Range
the three important metallogenic belts in the world and hosts numerous in the southern Altaids (Xiao et al., 2004a,b). The East Tianshan
⁎ Corresponding author at: Key Laboratory of Mineral Resource, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China.
E-mail address: cm-han@mail.iggcas.ac.cn (C. Han).
https://doi.org/10.1016/j.jseaes.2018.05.001
Received 16 November 2017; Received in revised form 1 May 2018; Accepted 2 May 2018
Available online 03 May 2018
1367-9120/ © 2018 Published by Elsevier Ltd.
C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
Fig. 1. Tectonic setting and distribution of significant deposits of the Eastern Tianshan Orogenic Belt, NW China (modified after Han et al., 2010; Deng et al., 2017).
polymetallic belt is one of the important producers of Cu–Au–Ni–Fe–Ag approximately east-west-trending faults, including the regional-scale
in China (Han et al., 2006; Fig. 2). The porphyry Cu deposits were Kalamaili-Maiqinwula, Kanggur, Yamansu, Aqikuduke and Xingxingxia
considered to be related to the late evolutionary stages of a subduction- faults, and many small-scale faults (Fig. 1; He et al., 1994; Xiao et al.,
related oceanic or continental magmatic arc (Mao et al., 2011). The 2004a,b). Of these faults, the Kangguer fault is the most prominent one,
province also contains post-collisional metallic mineral deposits formed consisting of mylonite, tectono-clastic rocks, tectonic lenses, and
between 280 and 240Ma (Zhang et al., 2005a,b). breccia, and which not only forms the boundary between the Ka-
The Donggebi is the largest, and economically the most important, zakhsta-Juanggar block and the Tarim craton, but is also an important
deposit in the Eastern Tianshan Orogenic Belt, with total Mo metal structural zone along which major magmatic activities and associated
reserves of 0.50 Mt (Huang et al., 2011a). It was discovered in 2008 and ore mineralization took place (He et al., 1994).
explored during the period 2009–2010; construction of the now-oper- Two distinct belts separated by the Kangguer fault can be re-
ating mine began in 2011. Since the discovery of the deposit, many cognized. The belt located north of the Kangguer deep-crustal fault is
scientific studies have been conducted that have addressed the geology interpreted as an arc, named the Dananhu-Tousuquan magmatic arc
and geochemistry of the deposit (Wang, 2011; Tu et al., 2011; Huang (He et al., 1994; Ji et al., 1994; Guo, 2000), which consists mainly of
et al., 2011a,b; Wu et al., 2017a,b), as well as the geological and geo- Middle Devonian to Carboniferous volcanic rocks, and contains several
chemical characteristics of the ore-forming granite porphyry (Yang porphyry Cu deposits of different sizes, including the Yandong, Tuwu,
et al., 2011; Deng, 2012). However, the documentation of the Donggebi Linglong and Chihu deposits (Fig. 1; Zhang et al., 2002). The southern
deposit has been reported in the Chinese literature, and therefore the belt is located between the Kangguer and Aqikekudouke faults, and is
international geological community knows little about this deposit until also interpreted as an arc, named Aqishan-Yamansu magmatic arc (Ji
now. In this contribution, we provide a detailed description of the the et al., 1994; Ma et al., 1997), which consists of Carboniferous rocks
Donggebi Mo deposit, together with new molybdenite Re-Os and zircon along the northern side of the Tarim craton, including the Early car-
U-Pb ages and S isotope compositions. Our results will be used to boniferous Aqishan and Yamansu Formations, and gray-wackes of the
constrain the timing of mineralization and possible sources of sulfur Middle Carboniferous Kushui Formation, separated by the Yamansu (or
and metals of the the Donggebi deposit. Kushui) Fault. It hosts numerous Fe, Cu, Au and Ag ore deposits. Re-
presentative of these are the Yamansu volcanic Cu–Fe deposit, the
2. Regional geological setting Weiquan Cu–Ag skarn deposit and the Lubaishan volcanic Cu deposit
(Fig. 1).
The Eastern Tianshan Orogenic Belt (Fig. 1) contains a number of The Kangguer fault separates Aqishan-Yamansu arc from the
Paleozoic terranes that amalgamated between the Siberian and Tarim Tousuquan-Dananhu magmatic arc to the north, and is considered to
cratons, and underwent complex tectonic evolution (Coleman, 1989; represent a Late Carboniferous to Early Permian suture, along which
Windley et al., 1990; Şengör et al., 1993; Şengör and Natal'in 1996; folding and thrusting within the arc sequences occurred during the
Xiao et al., 2004a,b). The tectonic history of the eastern Tianshan subduction of a Paleo-Tianshan ocean (Ji et al., 1994; Ma et al., 1997;
orogenic belt is considered to have been associated with the evolution Mao et al., 2002;Wu et al.,2014). By the end of the Carboniferous, an
of an ancient Tianshan ocean between the Tarim craton and the extensional tectonic regime developed along the major faults and the
Junggar-Kazakhstan block (Allen et al., 1993; Şengör et al., 1993; Kangguer orogenic lode deposits formed along some brittle-ductile
Şengör and Natal'in 1996; Xiao et al., 2004a,b;Deng et al., 2016, 2017). shear zones within subordinate faults, which represent dilatational
The orogen is separated from the Tarim craton to the south by the zones that were opened along an east-west-trending extension (Mao
Kanggguer ductile suture zone, and extends west to Gansu Province. et al., 2002).
The main structures of East Tianshan is characterized by a series of
271
C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
93°18′25″ 93°22′01″
A'
ZK0716
ZK1100
DGB12-8
DGB12-7 ZK70
ZK0300 ZK0312
Quaternary
sediment
DGB12-4 ZK0404
ZK1
ZK3
ZK1200
Metamorphic volcanic rocks A
Gandun Fm., Early Carboniferous
  Fault
mansu
 
Metamorphic pelite/sandstone, Ya 500m
Gandun Fm., Early Carboniferous
93°18′25″ 93°22′01″
Quaternary sediment Diabase dyke Fault Sampling drill
Metamorphic pelite/sandstone, 
Gandun Fm., Early Carboniferous Anticline
Metamorphic volcanic rocks
Gandun Fm., Early Carboniferous Quartz vein Syncline ZK1  Drill and numbered
Fig. 2. Geological map of the the Donggebi Mo deposit (After Deng, 2012).
3. Deposit Geology fracture zone is recognized, hosting the main mineralization, which
trends NE and dip southeast with an angle of 30–60° (Fig. 3).
The Donggebi deposit is mostly concealed by Quaternary over- A total of five mineralized bodies have been identified, and they are
burden and is mainly hosted in the Lower Carboniferous Gandun distributed in the contact zone between porphyritic granite and meta-
Formation (Fig. 2). The Gandun Formation is composed of meta-sand- sedimentary rocks of the Lower Carboniferous Gandun Formation.
stone, meta-sandy mudstone, meta-argillaceous sandstone, meta-mud- Individual ore bodies vary from 280m to 851m in length and 10m to
stone, silicalite, tourmalite, meta andesite, tuff and hornfels. The stra- 64.7 m in thickness. In the dipping direction, the explored ore bodies
tigraphic units trend WNW and dip ENE with an angle of 50–75°. The extend over 319m below the surface (Fig. 3). The main ore bodies trend
sedimentary rocks are thermometamorphically overprinted by deeper- in NE direction with a dip angle of about 30° (see Fig. 4).
seated intrusive rocks. Principal metallic minerals are molybdenite and pyrite with minor
No intrusions are exposed at surface near the deposit, but several quantities of chalcopyrite, galena, magnetite, scheelite and wolframite
intrusive stocks and/or dikes, including porphyritic granite, granite (Fig. 5). The gangue minerals include mainly orthoclase, plagioclase
porphyry, have been intersected in drill holes. Some granite porphyries and quartz, with lesser amounts of calcite, muscovite and chlorite. The
occur as dikes in the mineralized area. An unmineralized biotite granite size of the molybdenite ranges from 0.03mm to 3.00mm. The ores are
is emplaced in the northwestern part of the mining area. The Donggebi characterized by euhedral and subhedra textures, veinlet-disseminated
intrusion is composed of porphyritic granite and granite porphyry and brecciated structures (Fig. 6)
(Fig. 4). The coarse-grained porphyritic granite generally contains Based on chemical and mineralogical analyses, several stages of
2–9% orthoclase, 6–51% plagioclase, 20–35% quartz, and 1–3% biotite, hydrothermal alternation are recognized at the Donggebi. The highest
with minor amounts of muscovite and sericite. Plagioclase crystals are Mo values occur in zones with complex hydrothermal overprinting. A
often replaced by granular saussurite and fine-grained clay minerals. potassic alternation (K-fsp+ secondary biotite) affected the entire mi-
The granite porphyry generally contains 30% orthoclase, 40% plagio- neralized area. It involved microcline growth in the matrix around and
clase, 25% quartz, and 5% biotite, with minor amounts of apatite, between biotite and plagioclase. Minor discrete disseminated pyrite and
muscovite and chlorite. The orthoclase crystals range from 0.51 to magnetite, and veinlets of magnetite ± pyrite are present in the po-
1.00mm in size. Alteration mineral include saussurite, sericite and tassic alternation zones (see Fig. 7).
chlorite. A zircon SHRIMP U-Pb age of 227.6 ± 1.3Ma recently ob- Light-coloured, almost white, irregular, phyllic (quartz-sericite/
tained from a porphyritic granite (Huang et al., 2011a). A stratabound- muscovite) alternation zones, overprint potassic alternation where
272
41°56′04″ 41°54′01″
41°56′04″ 41°54′01″
C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
ZK3
A ZK1200 ZK1 ZK404 ZK0300 ZK0312 ZK70 ZK1100 ZK1500 ZK1900 A′
800m
DGB-12
DGB-13
258.02m DGB-11
600m
340.65m DGB-16
DGB-14
DGB-15
397.30m
436.28m
441.08m DGB-17
500.20m 400m
529.80m
DGB-18
0 100 200m
669.26m 200m
720.30m
729.30m
Porphyry granite Carboniferous Gandun Formation ZK3 Borehole and numbered
Oxidized Mo Ore Primary Mo  Ore Sample location
Fig. 3. Geological profile map of the the Donggebi Mo deposit (After Deng, 2012).
Fig. 4. Photographs of host rocks from the the
Donggebi deposit. (a) Meta-sandly mud (drill hole
ZK0303, depth 272m); (b) Meta-argillaceous
sandstone (drill hole ZK0302, depth 160.40m);
(c) Meta-mudstone (drill hole KZK0404, depth
26.00m); (d) Meta-sandstone (drill hole
KZK1108, depth 77.00m); (e) Propylitic altered
porphyritic granite (drill hole ZK0102, depth
540m); (f) Muscovitization porphyritic granite
(drill hole ZK0804, depth 184.80m); (g) K-feldspar-
quartz veinlet bearing granite porphyry (drill
hole KZK0404, depth 179.48m); (h) K-feldspar-
quartz-chalcopyrite-bearing muscovitization por-
phyritic granite (drill hole ZK0102,
depth 540m); Abbreviations. Kp=K-feldspar
phenocryst, Mu=muscovite, Mo=Molybdenite,
Cp=Chalcopyrite, Quartz, PG=porphyritic
granite, MSM=Meta sandy mud, MSS=
Metasandstone, MAS=Meta argillaceous,
MMS=Meta-mudstone.
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C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
Fig. 5. Photographs of some ore samples from the the Donggebi Mo deposit. (A) Molybdenite veinlets in quartz; (B) Massive pyrite in quartz; (C) Disseminate
chalcopyrite-sphalerite-galena in quartz vein; (D) Massive chalcopyrite in quartz; (E) Massive chalcopyrite-molybdenite in meta-sandstone; (F) Quartz, muscovite and
polysynthetic twin plagioclase of porphyritic granite, polarization microscope; (G) Quartz-potash feldspar vein; (H) Calcite-quartz vein; I-Chloritization biotite.
Abbreviations. Mo=Molybdenite, Qtz=Quartz, Py=Pyrite, Gn=Galena, Sp= Sphalerite Cp=Chalcopyrite, Bi= Biotite, Ch=Chlorite, MS=Muscovite,
Kfs=K-fedspar, Cal= Calcite.
sericite/muscovite together with fine-grained quartz have replaced all of which were collected from ZK0404, ZK0300 and ZK0312.
feldspar. Euhedral pyrite is common in this zone, whereas minor Sampling locations are marked in Fig. 2. Gravitational and magnetical
chalcopyrite occurs with disseminated molybdenite. Silicification (silica separation was applied and then handpicked under a binocular micro-
flooding) with fine-grained quartz is associated with stockwork quartz scope (purity > 99%). The molybdenite in the samples is fine grained
veins and veinlets with chalcopyrite, pyrite, molybdenite, and magne- (< 0.1mm), thus avoiding the decoupling of Re and Os within large
tite. Weakly developed biotitization zone, related to late-stage vein molybdenite grains (Stein et al., 1997).
composed of quartz and biotite and associated with minor Mo orebodies Re-Os isotopic analyses were performed at the National Research
is hosted in this zone. Center of Geoanalysis, Chinese Academy of Geosciences. Details of the
According to mineral assemblages and crosscutting relationships of chemical procedure are giving in Du et al. (1995, 2001), Shirey and
the ore veins, five mineralization stages can be identified (Fig. 8). Stage Walker (1995), Stein et al. (1997), and Markey et al. (1998) and are
I is characterized by K-feldspar and quartz veins; and wolframite also briefly described here.
formed during this stage. Stage II is an assemblage consisting of quartz, The Carius tube (a thick-walled borosilicate glass ampoule) diges-
magnetite, and a little molybdenite. Stage III (main mineralization tion technique was used. The weighed sample was loaded in a Carius
stage) consists of molybdenite, chalcopyrite and pyrite, with minor tube through a long thin-neck funnel. The mixed 190Os and 185Re spike
galena and sphalerite. Stage IV is marked by the formation of the calcite solution and 2ml of 10 N HCl and 6ml of 16 N HNO3 were added while
and gypsum. the bottom part of the tube was frozen at −80 to −50 °C in an ethanol-
liquid nitrogen slush and the top sealed using an oxygen-propane torch.
The tube was then placed in a stainless-steel jacket and heated for 10 h
4. Samples and analytical methods at 230 °C. Upon cooling, the bottom part of the tube was kept frozen,
the neck of the tube was broken, and the contents of the tube were
4.1. Re-Os molybdenite dating poured into a distillation flask after which the residue was washed out
with 40ml of water.
We selected 8 samples from the Donggebi deposit for Re–Os dating,
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C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
(caption on next page)
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C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
Fig. 6. Typical ore texture and structure in the the Donggebi Mo deposit. (A) Subhedral - allotriomorphic granular pyrite and allotriomorphic molybdenum; (B)
Molybdenum vein presented in the quartz vein; (C) Foliated molybdenum occurred in the quartz vein; (D) Euhedral-subhedral granular pyrite; (E) Disseminated
chalcopyrite and euhedral pyrite; (F) Massive ore sample consisting chalcopyrite and pyrite, and sphalerite vein present metasomatic structure in chalcopyrite; (G)
Euhedral-subhedral granular pyrite and chalcopyrite in a eutectic texture; (H) Disseminated chalcopyrite occurring in the sphalerite, and some chalcopyrite present a
euhedral-subhedral texture; (I) Euhedral pyrite in a cataclastic structure; (J) Galena and pyrite presented a eutectic texture; (K) Disseminated chalcopyrite in the
metasandstone; (L) Pyrite veinlet in the metasandstone; (M) Occurrence of banded and massive pyrite in the meta-mudstone; (N) Molybdenum veinlet in a quartz
vein; (O) Massive pyrite in the metasandstone; (P) Sparse disseminated pyrite occurring in quartz vein; (Q) Disseminated pyrite in the porphyritic granite; (R) Massive
pyrite present in metasandstone. Abbreviations. Py=Pyrite, Mo=Molybdenite, Cp=Chalcopyrite, Sp= Sphalerite, Qtz=Quartz, MSS=Metasandstone,
Gn=Galena, Ang= anglesite.
Separation of osmium by distillation and separation of rhenium by 4.3. Sulfur isotope analyses
extraction was performed based on the analytical method in Du et al.
(2001). A TJA PQ-EXCELL ICP-MS was used for the determination of Twenty-two sulfide samples including molybdenite, pyrite and
the Re and Os isotope ratio. chalcopyrite were selected from different parts of orebodies for sulfur
Average blanks for the total Carius tube procedure were ca. 10 pg Re isotope analyses, there are collected from Stage III (main mineralization
and ca. 1 pg Os. The analytical reliability was tested by repeated ana- stage). Sulfide-bearing veins/veinlets were first cut from their host
lyses of molybdenite standard HLP-5 from a carbonatite vein-type rocks and crushed to 40 to 80 mesh; sulfide minerals were then hand-
molybdenum-lead deposit in the Jinduicheng-Huanglongpu area of picked under a binocular microscope to remove impurities. Sulfide se-
Shaanxi Province, China. Fifteen samples were analyzed over a period parates were then crushed to<200-mesh powder in an agate mortar.
of 5months. The uncertainty in each individual age determination was Sulfur isotope analyses were completed using a Finnigan MAT-252 mass
about 0.35% including the uncertainty of the decay constant of 187Re, spectrometer according to the method of Ueda and Sakai (1984), at the
isotope ratio measurement, and spike calibrations. The average Re-Os Institute of Geology and Geophysics, Chinese Academy of Sciences in
age for HLP-5 is 221.3 ± 0.3Ma (95% confidence limit, Stein et al. Beijing. The sulfide powder was enclosed in a tin cup and then put in a
1997). Median age and mean absolute deviation were reacting furnace. Subsequently, the powder was oxidized to SO2(g).
221.34 ± 0.12Ma. The average Re concentration was Helium was used as a carrier gas and mixed with SO2 to facilitate
283.71 ± 1.54 μg/g, while the average Os concentration was transport into the mass spectrometer. Reference standards GBW04414
657.95 ± 4.74 ng/g. and GBW04415 were used as external standards to calibrate the sulfur
isotope composition of unknown samples. During our analytical ses-
sion, the obtained δ34S values are −0.10 ± 0.17‰ (2σ; n=12) for
4.2. Zircon U-Pb dating standard GBW04414, consistent with its recommended value of
−0.07 ± 0.13‰ (2σ; Ding et al., 2001). The analytical precision is
Sample DGB12-4, DGB12-7 and DGB 12-8 are porphyritic granite, typically± 0.2‰ (2σ).
collected from the Donggebi porphyry Mo deposit, sample DGB12-4
(41°54′52″N, 93°20′43″E) collected from ZK0404, sample DGB12-7 5. Results
(41°54′55″N, 93°20′45″E) collected from ZK0300 and sample DGB12-8
(41°54′58″N, 93°20′50″E) collected from ZK0312(Fig. 2). 5.1. Re-Os molybdenite ages
Zircons were separated using conventional heavy liquid and mag-
netic techniques and picked under a binocular microscope. The grains The concentrations of Re and Os and the osmium isotopic compo-
were mounted along with Temora standard and then cast in epoxy resin sitions of molybdenite from the Donggebi Mo deposit are shown in
in a 2.5 cm diameter mount and ground to expose the center of the Table 1. The total Re and Os concentrations of molybdenite range from
grains. Internal structures of zircon were examined using cath- 10 to 63 µg/g and 26 to 155 ng/g, respectively. Model ages for the
odoluminescence (CL) images prior to U–Pb analyses. In-situ zircon deposit were calculated assuming that the initial abundance of 187Os is
U–Pb ages were acquired on the Cameca IMS-1280 ion microprobe zero. Isochron ages for all samples from the Donggebi Mo deposit were
(SIMS) in single collector mode at the Institute of Geology and calculated using Isoplot Model 3 with 2% input error. The numbers
Geophysics (IGG), Chinese Academy of Sciences, Beijing. The U–Th–Pb within the brackets in Table 1 are measurement errors, and correspond
ratios and absolute abundances were determined relative to the stan- to the last digit of analytical data in front of the brackets. A regression
dard zircon 91,500 (Wiedenbeck et al., 1995), analyses which were analysis was applied to 8 analytical data of molybdenite, which yields
interspersed with those of unknown grains, using operating and data an isochron age of 234.3 ± 1.6Ma (2σ) with an initial 187Os of
processing procedures similar to those described by Li et al. (2009). The 0.04 ± 0.45 (MSWD=0.25) (Fig. 9), identical to the mean age
mass resolution used to measure the Pb/Pb and Pb/U isotopic ratios (234.4 ± 1.2Ma,± 0.50% 2σ, n=8) calculated from the single
was 5400 during the analyses. A long-term uncertainty of 1.5% (1RSD) sample age determination (Fig. 10). Model ages for individual analyses
for 206Pb/238U measurements of the standard zircons was propagated range from 233.7 ± 3.2 to 235.6 ± 3.4Ma (Table 1).
to the unknowns (Li et al., 2010). Despite that the measured 206Pb/238U
error in a specific session was generally around 1% (1RSD) or less. 5.2. Zircon U-Pb geochronology
Measured compositions were corrected for common Pb using non-
radiogenic 204Pb. Corrections were sufficiently small to be insensitive to Zircons from three samples of porphyritic granite were dated using
the choice of common Pb composition, and an average of present-day the U-Pb technique in order to constrain the age of the main stage of
crustal composition (Stacey and Kramers, 1975) was used, assuming magmatism. Fig. 10 shows representative cathodoluminescence (CL)-
that the common Pb is largely surface contamination introduced during SEM images of zircon types from the porphyritic granite. The zircons
sample preparation. Uncertainties on individual analyses in data tables have grain sizes from 50 μm to 200 μm. They are short, euhedral prisms,
are reported at a 1σ level; mean ages for pooled U/Pb (and Pb/Pb) which in many cases have well-developed oscillatory zoning without
analyses are quoted with 95% confidence interval. Data reduction was distinctively older cores and younger overgrowths in the CL images
carried out using the Isoplot/Ex v. 2.49 program (Ludwig 2001). (Fig. 10). SIMS zircon U-Pb data for the Donggebi intrusion are pre-
sented in the Table 2.
Thirty-nine analyses on 39 zircons from three samples (DGB12-4,
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C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
(caption on next page)
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C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
Fig. 7. Wall rock alteration in the the Donggebi Mo deposit. (A) K-feldspar alternation in the metasandstone; (B) Silicification, pyrite and chalcopyrite in quartz veins;
(C) K-feldspar alternation and silicification in the metasandstone; (D) Silicification, disseminated molybdenite in quartz vein; (E) K-feldspar alternation and silifi-
cation present in the metamudstone; (F) Silicification, the multi-phase quartz veins in the granite are interrelated with the fluorite vein ; (G) Silicification, fluorite-
quartz veins developed in pyrite and chalcopyrite; (H) Silicification, the quartz vein in the porphyritic granite, and chalcopyrite in quartz vein; (I) Silicification and
carbonatization, quartz - calcite vein present in the metasandstone; (J) Silicification, a quartz vein developed in metasandstone; (K) feldspar alternation and
silification present in the metamudstone; (L) Silicification and carbonatization, quartz and calcite veins in the metamudstone; (M) Silicification and carbonatization,
late calcite vein crosscutting earlier formed quartz vein; (N) Plagioclase with sericitization; (O) Metasandstone with sericitization; (P) Metamudstone with muscovite
alternation and chloritizatio; (Q) Amphibole with chloritization. Abbreviations.Kfs= K-fedspar, Cp=Chalcopyrite, Py= Pyrite, Qtz=Quartz,
MSS=Metasandstone, Cal= Calcite, Pl= Plagioclase, Ch=Chlorite, MS=Muscovite, Bi=Biotite, Amp=Amphibole, Mo=Molybdenite,
236.2 ± 3.3Ma (95% confidence level, MSWD=0.38, n= 14;
Minerals Stage 1 Stage 2 Stage 3 Stage 4 Fig. 11b). Eleven spot analyses on 11 zircon grains from sample DGB12-
K-feldspar 8 yielded concordant
206Pb/238U ages that range between 238.6 ± 3.7
and 231.7 ± 3.4Ma, with a weighed mean of 236.3 ± 3.2Ma (95%
Wolframite confidence level, MSWD=0.23, n=11; Fig. 11c).
Pyrite
5.3. Sulfur isotope compositions of sulfide minerals
Chalcopyrite
The δ34S values of sulfides are presented in Table 3, and range from
Magnetite
1.5 to 3.8‰, with an average value of 2.81 ± 2.24‰ (n=22), sig-
Scheelite nificantly higher than those of the mantle (0 ± 3‰) and most por-
phyry systems (0 ± 5‰), suggesting that a 34S-enriched sulfur source
Quartz contributed to at least part of the the Donggebi sulfur inventory. Eight
Molybdenite molybdenite samples recorded a broad range of δ34S values varying
from 3.36 to 3.86‰ (n=8, mean=3.64 ± 0.11‰), whereas the
Sphalerite ranges of δ34S values for other sulfides are more restricted, i.e., 2.3 to
Galena 3.1‰ (n=4, mean= 2.76 ± 0.31‰) for pyrite and 1.54 to 2.43‰
(n=10, mean=2.02 ± 0.35‰) for chalcopyrite.
Calcite
Gypsum 6. Discussions
Fig. 8. Paragenesis sequence of minerals of the the Donggebi Mo deposit 6.1. Source of ore-forming metals
(modified from Deng, 2012).
It is well known that post-collisional granitoids form some of the
DGB12-7, DGB12-8) were obtained. Zircons from the porphyritic largest volumes of granite in orogenic belts. Moreover, mantle sourced
granite are mostly euhedral and colourless. In CL images (Fig. 10), no mafic magma contributions play an important role in their evolution.
inherited cores were observed. The zircons have high uranium (from Recent studies show that I-type and A-type Central Anatolian granitoids
205 to 1647 ppm) and Th (from 108 to 1211 ppm) contents, and high are good examples of post-collisional granitoids in the Alpine orogenic
Th/U ratios (from 0.40 to 1.38) (Table 2). Such features indicate that belt and show geochemical evidence of mantle-derived mafic magma
they were crystallized from magmas (Wu et al., 2006). contributions (Delibaş, 2009; Delibaş et al., 2011). However, mafic
Fourteen spot analyses on 15 zircon grains from sample DGB12-4 magma contributions in the evolution of post-magmatic ore occur-
yielded concordant 206Pb/238U ages that range between 239.0 ± 3.5 rences/deposits have not been known in the Central Asia Orogenic Belt.
and 232.1 ± 3.5Ma, with a weighted mean of 236.4 ± 2.7Ma (95% In recent years, the Re contents of the molybdenites have been used to
confidence level, mean square weighted deviation [MSWD] = 0.36, trace the source of ore materials (Mao et al., 1999, 2003, 2006). The
n=14; Fig. 11a). Fourteen spot analyses on 13 zircon grains from Rhenium content in molybdenites decreases gradually in the order;
sample DGB12-7 yielded concordant 206Pb/238U ages that range be- mantle source> a mixture of mantle and crust> crustal source (Mao
tween 239.5 ± 3.8 and 231.9 ± 3.4Ma, with a weighed mean of et al., 1999, 2003, 2006). In addition, concluded that deposits with
mantle components (e.g., mantle underplating, mantle metasomatism,
Table 1
Re-Os isotopic data for molybdenite from the Donggebi Mo deposit, easternTianshan.
No.samples Weight (g) Re (μg/g) 187 187Re (μg/g) Os (μg/g) Model age (Ma)
Measured 2σ Measured 2σ Measured 2σ Measured 2σ
DGB-12 0.02052 33.12 0.27 20.82 0.17 81.37 0.72 234.1 3.4
DGB-11 0.05034 41.97 0.31 26.38 0.19 103.8 0.90 235.6 3.4
DGB-13 0.05056 10.92 0.09 6.862 0.06 26.87 0.26 234.6 3.5
DGB-14 0.05018 38.24 0.32 24.03 0.20 93.91 0.78 234.1 3.3
DGB-15 0.05008 59.27 0.52 37.25 0.33 146.0 1.20 234.8 3.4
DGB-16 0.05012 41.03 0.34 25.79 0.21 101.0 0.80 234.7 3.3
DGB-17 0.05025 56.39 0.45 35.44 0.28 138.2 1.10 233.7 3.2
DGB-18 0.05015 63.18 0.56 39.71 0.35 154.9 1.30 233.7 3.4
Enriched 190Os and 185Re were obtained from the Oak Ridge National Laboratory. Decay constant:λ (187Re)= 1.666×10−11/year (Smoliar et al., 1996). The
uncertainty in each individual age determination was about 0.35% including the uncertainty of the decay constant of 187Re, uncertainty in isotope ratio mea-
surement, and spike calibration.
278
C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
240 200
238
160
236
120
234
80
232
40 Age = 234.3 ± 1.6 Ma
230 187
Mean = 234.4 ±1.2 Ma [0.50%]  95% conf. Initial Os ng/g =0.04 ± 0.45
Wtd by data-point errors only MSWD = 0.25
MSWD = 0.15, probability = 0.994
228 00 10000 20000 30000 40000 50000
187Re ng/g
Fig. 9. (a) Re-Os weighted average model age diagram; (b) Isochron diagram for molybdenite samples from the the Donggebi Mo deposit. The Re-Os ages are listed in
Table 2.
Fig. 10. Cathodolumninescence (CL) imagines of zircons from porphyritic granite of the Donggebi Mo deposit. Circles show the locations of SIMS U-Pb age isotope
measurement, 206Pb/238U(Ma) are shown above the circles. Numbers refer to spots listed in the Table 3. a-DGB-4, b-DGB-7, c-DGB-8,
melting of mafic or ultramafic rocks) have higher Re contents, whereas (crust+mantle) origin, but crustal components are more dominant.
deposits of crustal origin have lower Re contents associated with mo- In general, δ34Ssulfide values for most porphyry-type deposits in the
lybdenites. In comparison to cited publications for different locations world range from −5 to 5‰, which are roughly consistent with the
(e.g., Mao et al., 1999, 2003, 2005), the relatively lower Re contents of accepted mantle range (0 ± 3‰). Our results show that most of the
molybdenites from the Donggebi Mo deposit may indicate a mixed sulfides from the Donggebi have δ34Ssulfide lower than 5.0‰, and
279
Age (Ma)
187Os ng/g
C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
Table 2
ZirconU-Pb data determined by monocollector SIMS mode of porphyritic granite from the Donggebi Mo deposit.
Sample spot Th/(ppm) U/(ppm) Th/U 207Pb/206Pb 1σ 207Pb/235U 1σ 206P/238U 1σ 207Pb/206Pb 1σ 207Pb/235U 1σ 206Pb/238U 1σ
DGB12-4
@1 960 1382 0.70 0.0519 1.01 0.2627 1.81 0.0367 1.50 283.0 23.0 236.8 3.8 232.2 3.4
@2 143 288 0.50 0.0498 3.65 0.2565 3.97 0.0374 1.57 186.0 82.8 231.9 8.3 236.4 3.6
@3 195 340 0.58 0.0509 2.26 0.2650 2.76 0.0378 1.58 236.3 51.3 238.7 5.9 238.9 3.7
@4 273 476 0.57 0.0509 2.71 0.2581 3.11 0.0368 1.51 234.8 61.5 233.2 6.5 233.0 3.5
@5 426 880 0.48 0.0502 1.67 0.2545 2.25 0.0368 1.50 202.6 38.4 230.2 4.6 233.0 3.4
@6 625 1037 0.60 0.0505 1.77 0.2640 2.32 0.0379 1.50 219.0 40.4 237.9 4.9 239.8 3.5
@7 349 580 0.60 0.0514 1.51 0.2631 2.13 0.0371 1.50 259.7 34.3 237.1 4.5 234.9 3.5
@8 470 539 0.87 0.0513 2.12 0.2617 2.60 0.0370 1.51 253.0 48.1 236.1 5.5 234.4 3.5
@9 614 1281 0.48 0.0508 1.24 0.2588 2.02 0.0370 1.60 229.5 28.3 233.7 4.2 234.1 3.7
@10 192 250 0.77 0.0516 2.29 0.2678 2.75 0.0377 1.52 266.2 51.7 241.0 5.9 238.4 3.6
@11 743 1245 0.60 0.0510 1.94 0.2657 2.45 0.0378 1.51 241.6 44.1 239.3 5.2 239.0 3.5
@12 443 553 0.80 0.0503 2.17 0.2608 2.64 0.0376 1.50 208.6 49.5 235.3 5.6 238.0 3.5
@13 683 728 0.94 0.0516 1.68 0.2634 2.28 0.0370 1.54 268.2 38.1 237.4 4.8 234.3 3.5
@14 233 342 0.68 0.0530 2.24 0.2680 2.70 0.0367 1.52 329.5 50.0 241.1 5.8 232.1 3.5
DGB12-7
@1 108 289 0.38 0.0502 3.25 0.25603 3.67 0.0370 1.71 204.2 73.8 231.5 7.6 234.2 3.9
@2 219 256 0.85 0.0532 2.19 0.27112 2.73 0.0370 1.63 337.0 49.0 243.6 5.9 234.0 3.7
@3 179 390 0.46 0.0515 1.79 0.26276 2.34 0.0370 1.51 263.7 40.5 236.9 5.0 234.2 3.5
@4 236 519 0.45 0.0506 2.32 0.25745 2.77 0.0369 1.51 221.4 52.8 232.6 5.8 233.7 3.5
@5 130 207 0.63 0.0502 4.94 0.25334 5.16 0.0366 1.51 202.2 110.7 229.3 10.7 231.9 3.4
@6 198 318 0.62 0.0509 1.99 0.26298 2.51 0.0374 1.53 237.7 45.3 237.1 5.3 237.0 3.6
@7 686 497 1.38 0.0504 1.91 0.25780 2.43 0.0371 1.50 214.6 43.6 232.9 5.1 234.7 3.5
Sample spot Th/ppm U/ppm Th/U 207Pb/206Pb 1σ 207Pb/235U 1σ 206P/238U 1σ 207Pb/206Pb 1σ 207Pb/235U 1σ 206Pb/238U 1σ
DGB12-7
@8 308 373 0.82 0.0515 2.60 0.26651 3.01 0.0375 1.52 263.3 58.7 239.9 6.5 237.5 3.5
@9 308 573 0.54 0.0516 1.72 0.26439 2.29 0.0372 1.51 267.5 38.9 238.2 4.9 235.2 3.5
@10 206 347 0.59 0.0519 2.07 0.26177 2.56 0.0366 1.52 281.3 46.6 236.1 5.4 231.6 3.5
@11 238 425 0.56 0.0510 1.69 0.26629 2.33 0.0379 1.60 241.7 38.5 239.7 5.0 239.5 3.8
@12 136 257 0.53 0.0539 2.70 0.27407 3.17 0.0369 1.65 366.3 59.8 245.9 6.9 233.5 3.8
@13 212 355 0.60 0.0517 3.56 0.26322 3.87 0.0369 1.52 271.9 79.5 237.3 8.2 233.8 3.5
@14 212 402 0.53 0.0512 2.90 0.26248 3.27 0.0371 1.51 252.1 65.3 236.7 6.9 235.1 3.5
DGB12-8
@1 385 568 0.68 0.0506 2.16 0.25855 2.64 0.0371 1.51 221.0 49.3 233.5 5.5 234.7 3.5
@2 443 839 0.53 0.0504 1.74 0.26226 2.35 0.0377 1.58 215.7 39.7 236.5 5.0 238.6 3.7
@3 275 509 0.54 0.0512 2.06 0.26375 2.55 0.0373 1.51 250.6 46.8 237.7 5.4 236.4 3.5
@4 295 540 0.55 0.0512 2.21 0.25852 2.69 0.0366 1.53 249.2 50.0 233.5 5.6 231.9 3.5
@5 130 225 0.58 0.0529 3.84 0.26777 4.12 0.0367 1.51 325.9 84.9 240.9 8.9 232.3 3.4
@6 518 826 0.63 0.0504 1.68 0.25905 2.26 0.0373 1.51 212.0 38.5 233.9 4.7 236.1 3.5
@7 181 256 0.71 0.0521 3.21 0.26681 3.55 0.0371 1.51 290.3 71.7 240.1 7.6 235.0 3.5
@8 177 244 0.73 0.0511 3.18 0.25770 3.52 0.0366 1.50 244.6 71.6 232.8 7.3 231.7 3.4
@9 1211 1647 0.74 0.0516 0.90 0.26588 1.78 0.0374 1.53 266.6 20.5 239.4 3.8 236.6 3.6
@10 294 737 0.40 0.0513 1.77 0.26234 2.32 0.0371 1.51 252.1 40.2 236.6 4.9 235.0 3.5
@11 458 556 0.82 0.0509 2.20 0.26008 2.67 0.0370 1.50 237.6 50.0 234.7 5.6 234.4 3.5
molybdenite and pyrite from early stages in the paragenesis (i.e., Stages depositional age of molybdenite. For the Donggebi Mo ore deposit, the
II and III) generally have higher δ34Ssulfide than those of pyrite and analysis of eight molybdenite samples yielded an isochron age of
chalcopyrite from later stages. These relatively high δ34Ssulfide values 234.3 ± 1.6Ma (2σ) with an initial 187Os of 0.04 ± 0.45. It is shown
could either be inherited from the magmatic source, or resulted from that the initial 187Os values from the molybdenite samples are close to
contamination by crustal marine sedimentary facies or evaporites with zero and the Re-Os isochron ages reflect the time of sulfide deposition.
high δ34Ssulfide values. Due to the fact that no marine evaporites or The Mo mineralization of the Donggebi Mo deposit took place after
carbonates have been reported near the Donggebi deposit, and that the regional low-grade metamorphism and folding, and was not influenced
Tuwu porphyry Cu deposit in this region has generally lower δ34Ssulfide by later geological events.
values (−0.9 to +1.3‰; Han et al., 2006), we therefore suggest that Mineralization in the eastern Tianshan, reported by some re-
the relatively lower δ34Ssulfide values of the sulfides from the Donggebi searchers (Mao et al. 2003; Han et al., 2010), is mainly of Late Paleo-
were probably inherited from a deep crustal material or the upper zoic age (330–260Ma). Younger mineralization ages from the In-
mantle. dosinian epoch (Mesozoic) have rarely been reported in the literature.
However, recent studies indicate that the ages of the Jinwuozi gold
6.2. Age of mineralization and its geological significance deposit are 228–230Ma, the Au-bearing quartz vein III of the
Shiyingtan gold deposit is 244 ± 9Ma, the Xiaobaishitou W-Mo de-
The Re-Os geochronometer, applied to molybdenite, has been de- posit yield Re-Os isotope model ages range from 239.7 ± 3.6Ma to
monstrated to be remarkably robust, even in situations of overprint by 251.4 ± 3.6Ma(Deng et al., 2017), and the Baishan Re-Mo deposit are
metamorphism and deformation. If molybdenite does not contain any between 225 and 233Ma (Zhang et al., 2005a,b) .
initial or common Os, all measured Os is monoisotopic (187Os) as the Similarly, some ages of 244–215Ma of metal deposits in the Beishan
product of decay of 187Re, and the isochron age then represents the have been reported (Liu et al., 2003). These ages are close to the Re-Os
280
C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
(a) 6.3. Ore-forming geodynamical settingDGB12-4
0.046
280 Almost all porphyry-style deposits described in the literature are
Phanerozoic and their formation is linked to magmatic activity at active
plate margins. They can be divided into two main types. porphyry Cu-
0.042 260 Mo and porphyry Cu-Au ± Mo deposits. The first type is generally
found in continental margin arcs, like the Andean belt, dominated by
calc-alkaline intrusions. The second type is typical of continental mar-
240 gins or island arc terranes, such as those in the southwest Pacific region0.038 where calc-alkaline rocks or high-K, calc-alkaline rocks prevail.
In the Rb against Y+Nb diagram (Fig. 12; Table 4), the Donggebi
220 porphyritic granites mainly show post-COLG characteristics. In this
0.034 case, ages of the Mo mineralization (234.3 ± 1.6Ma) and also ages
236.4±2.7Ma and tectonic setting of the host rocks (the Donggebi) reveal that Mo
MSWD=0.36
n=14 mineralization in the Eastern Tianshan Orogenic Belt occurred duringthe post-collisional setting. The Eastern Tiashan Orogenic Belt became
0.030
0.21 0.23 0.27 0.31 0.33 0.35 Angaran active continental margin before the Early Permian (Xiao0.25 0.29
235 et al., 2004a,b). Its geodynamic evolution was closely associated with207Pb/ U the evolution of an ancient Asian ocean, crustal thickening and com-
(b) DGB12-7 pressional tectonics occurred at Late Permian times, and after the early0.046 Triassic time the thin-skin extensional tectonics continued to stretch the
280 crust in the region (Xiao et al., 2004a,b).
Post-orogenic suites correspond to the last magmatic episodes in an
260 orogenic belt. Structural data from Permian to Triassic rocks in regions0.042 260 adjacent to Eastern Tianshan indicate extensive thrusting, strike-slip
faulting, and possibly also extension associated with the amalgamation
of different blocks (Lamb et al., 2008; Laurent-Charvet et al., 2003;
0.038 240 Wang et al., 2010). The existence of post-orogenic Triassic granitoids in
the Eastern Tianshan near to the western part of the Beishan region has
been used to support a change in geodynamic regime from Paleo-Asian
220 Ocean subduction-collision to the Paleo-Tethys Oceanic regime which
0.034 took place during the Late Permian to Early Triassic (Zhang et al.,
236.2±3.3Ma 2005a,b; Li et al., 2010). These regional studies reveal that the final
0.038 MSWD=0.38
n=14 amalgamation between the southern active margin of the Siberia
0.030 Craton and the passive margin of Tarim Craton, may have extended
0.21 0.23 0.25 0.27 0.29 0.31 0.33 0.35 from the end-Permian to Early Triassic (Xiao et al., 2004a,b). Therefore,
207Pb/235 we conclude that the mid-Triassic pluton in the Eastern Tianshan regionU was generated during this post-orogenic event.
DGB12-8 Many Triassic plutons have been recognized from the eastern part of0.046 (c) the CAOB and the northern parts of the North China Craton, and many
280 of them are distributed along collision belts between the southern
Mongolia arc terranes and the North China Craton (Chen et al., 2009; Li
0.042 et al., 2010; Wu et al., 2011). Our study now shows that similar Triassic260 plutons are also present in the Eastern Tianshan orogen, indicating that
Triassic magmatism extends into the south-central margin of the CAOB.
Triassic magmatic activity may therefore be more widespread than
0.038 240 previously considered.
In the CAOB, Triassic granitoids occur widely in the eastern seg-
ment, such as NE Mongolia, NE China and the Russian Far East
220
0.034 236.3±3.2Ma
(Transbaikalia), (Jahn et al., 2000, 2009; Wu et al., 2011; Yarmolyuk
MSWD=0.23 et al., 2002). These granitoids were predominately of syn-orogenic or
n=11 post-orogenic types and most likely related to Mesozoic subduction/
collision, such as the Transbaikal arc and Mongol-Okhotsk suturing, as
0.030 well as the Circum-Pacific arcs (Yarmolyuk et al., 2002). In the central
0.21 0.23 0.25 0.27 0.29 0.31 0.33 0.35 part of the CAOB, such as in central Mongolia (Jahn et al., 2009;
207Pb/235U Yarmolyuk et al., 2002), the Early to Middle Triassic intrusions were
also probably emplaced in a syn-orogenic or postorogenic setting. This
Fig. 11. Zircon U-Pb Concordia diagrams for the dated porphyritic granite of was related to the Mesozoic collision of the Baydrag and Hangay blocks
the Donggebi Mo deposit. (a) DGB-4, (b) DGB-7, (c) DGB-8, and Mongol-Okhotsk suturing (Badarch et al., 2002; Orolmaa et al.,
2008; Yarmolyuk et al., 2002). By contrast, further west in the CAOB,
ages (234Ma) of molybdenite from the Donggebi Mo deposit in the i.e., the Altai region, the Early Mesozoic granites were intruded in a
eastern Tianshan, and indicate that the Indosinian period is also an post-orogenic to anorogenic setting (Wang et al., 2010). However, in
important mineralization epoch in the eastern Tianshan orogenic belt. the Beishan orogen located at the mid-southern margin of the CAOB,
the Triassic plutons were mainly generated in a post-orogenic setting.
Therefore, the Early to Middle Triassic granitoids in the western and
eastern parts of the CAOB may record different tectonic settings (Li
281
206Pb/238U 206Pb/238U 206Pb/238U
C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
Table 3
Sulfur compositions of sulfide minerals from the Donggebi Mo deposit.
Sample No. Minerals δ34S 34CDT (‰) Sample No. Minerals δ SCDT (‰)
DGB-02 Chalcopyrite 1.94 DGB-12 Pyrite 3.08
Molybdenite 3.81 Chalcopyrite 2.14
DGB-03 Chalcopyrite 2.25 Molybdenite 3.75
Molybdenite 3.78 DGB-13 Chalcopyrite 1.70
DGB-04 Chalcopyrite 2.04 Pyrite 2.84
Molybdenite 3.61 DGB-14 Chalcopyrite 1.94
DGB-06 Chalcopyrite 2.22 Molybdenite 3.64
Pyrite, 2.34 DGB-16 Chalcopyrite 1.98
Molybdenite 3.57 Pyrite 2.78
DGB-09 Chalcopyrite 2.43 DGB-20 Chalcopyrite 1.54
Molybdenite 3.57 Molybdenite 3.36
et al., 2010). In other words, voluminous syn-orogenic granitoids occur
1000 in the eastern part (and at the southeastern margin), whereas there is
syn-COLG little anorogenic magmatism in the more western parts (and at the
southwestern margin). This provides evidence that the final phase of
WPG Paleo-Asian Ocean closure of the CAOB took place a gradual scissor-
100 post-COLG type closure from west to east.
7. Conclusions
10 VAG The Donggebi porphyry Mo deposit in the eastern Tianshan oro-
ORG genic belt is hosted in the Lower Carboniferous Gandun Formation
metasedimentary rocks. Five stages of mineralization are associated
with propylitic and phyllic alterations. Molybdenite mainly occurs in
1
2 10 100 1000 veins and veinlets that contain quartz, fluorite, magnetite, and pyrite,
(Y+Nb)ppm with minor chalcopyrite, sphalerite, and galena, and is associated with
phyllic alteration. Re-Os molybdenite dating results indicate that this
Fig. 12. The Rb against Y+Nb diagram of porphyritic granite from the the deposit formed at ∼234Ma, whereas SIMS U-Pb zircon age of
Donggebi Mo deposit. VAG=Volcano Arc Granite, Syn-COLG= Syncollision ∼236Ma for the porphyritic granite suggest that it was probably re-
Granite, WPG=Within-Plate Granite.ORG=Ocean Ridge granite. lated to the Triassic felsic magmatism in this area. Sulfur isotope data
for sulfide minerals, together with their paragenesis, suggest a mantle-
Table 4
Trace element compositions of porphyritic granite from the Donggebi Mo deposit.
Samples No. DGB-1 DGB-2 DGB-3 DGB-4 DGB-5 DGB-6 DGB-7 DGB-8 DGB-9 DGB-10 DGB-11
La 19.2 22.4 21.5 20.8 24.4 24 23.7 20.2 23.6 31.3 24.6
Ce 40.6 47.2 45.4 43.1 51.2 51.8 48.9 43.4 50 64.3 51
Pr 4.42 4.94 4.84 4.82 5.64 5.43 5.22 4.61 5.4 6.95 5.68
Nd 16.5 17.6 17.2 18.1 20.9 20.1 19 16.9 19.8 25.4 20.4
Sm 3.43 3.18 3.14 3.57 4.11 3.89 3.73 3.44 3.89 4.66 4.18
Eu 0.45 0.36 0.41 0.5 0.53 0.53 0.51 0.5 0.51 0.57 0.5
Gd 3.19 2.64 2.73 3.66 3.8 3.68 3.44 3.05 4.02 4.28 3.71
Tb 0.54 0.39 0.43 0.61 0.61 0.58 0.55 0.5 0.68 0.67 0.62
Dy 3.32 2.2 2.48 3.92 3.66 3.18 3.24 2.99 4.11 4 3.68
Ho 0.67 0.41 0.49 0.8 0.67 0.62 0.62 0.58 0.81 0.76 0.7
Er 2.17 1.4 1.57 2.65 2.21 1.94 2.08 1.84 2.71 2.43 2.24
Tm 0.34 0.23 0.26 0.43 0.37 0.31 0.32 0.28 0.43 0.37 0.37
Yb 2.55 1.64 1.91 3.05 2.6 2.26 2.25 2.03 3.04 2.7 2.68
Lu 0.39 0.26 0.32 0.44 0.4 0.34 0.35 0.31 0.47 0.42 0.41
Zr 104 110 103 116 116 112 118 108 105 115 112
Hf 4.2 4.36 4.17 4.2 4.45 4.24 4.19 4.24 4.11 4.49 4.29
Sc 4.66 3.39 4.24 5.1 5.51 5.01 6.24 4.16 5.05 5.16 7.85
Ga 17.8 16.4 17.6 18 17.8 17.7 19.1 17.5 17.7 19.4 22.3
Rb 363 309 345 367 305 303 326 331 436 428 363
Sr 109 96.5 104 87.7 146 147 128 136 68.8 96.7 116
Nb 16.7 26.2 36.6 15.5 15.7 17.7 19.3 15.5 16 17.8 16.6
Cs 25.9 24 26.9 26.6 21 21.2 26.6 23 26 25.8 34.1
Ba 323 281 307 244 328 361 346 384 262 332 276
Ta 2.26 4.71 7.13 1.87 2.09 2.43 2.24 1.98 2.04 2.05 1.84
Pb 20.2 23.9 18.5 21 23.5 24.5 22.2 23.7 23.2 25 18.9
Th 20.4 16.7 15.9 19.8 19.8 21.8 21.9 18.7 18.1 22.9 19.5
U 5.56 5.77 5.76 6.22 6.42 5.69 4.77 5.26 6.96 5.17 7.11
282
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like, magmatic signature for the early vein stages (including molybde- He, G.Q., Li, M.S., Liu, D.Q., Zhou, N.H., 1994, Palaeozoic Crustal Evolution and
nite), whereas later vein stages (containing chalcopyrite) recorded Mineralization in Xinjiang of China. Urumqi, Xinjiang People’s Publishing House, pp.
greater crustal signature. Combined with the regional geological his- 1–437.Huang, C.Y., Wu, B.Y., Weng, J.C., Li, W.Z., Xi, G.Z., Yuan, D.F., Zhao, X.B., 2011a.
tory, we conclude that the evolution of the porphyry Mo deposit in the Discovery of the Eastern Gobi Hugesize Molybdenum Ore Deposit and Its Prospecting
Donggebi area and associated Mo mineralization during early Mesozoic Significance in Eastern Tianshan. Geol. Survey Res. 34, 169–188 (in Chinese with
time were closely related to a post-collisional extensional setting. English abstract).Huang, C.Y., Lang, Y.F., Dong, L.Q., Fu, Z.G., 2011b. Geological characteristics and
genesis of the the Donggebi oversize molybdenum deposit in Eastern Tianshan. China
Acknowledgements Molybdenum Indust. 35, 8–17 (in Chinese with English abstract).
Jahn, B.-M., Wu, F.-Y., Chen, B., 2000. Granitoids of the Central Asian Orogenic Belt and
continental growth in the Phanerozoic. Transactions of the Royal Society of
We are indebted to Bin Cui, Jingwen Mao, Kezhang Qin, Zhaochong Edinburgh. Earth Sci. 91, 181–193.
Zhang, Yitian Wang, Jinyi Li, Tianlin Ma, Lian-Chang Zhang, Zhiliang Jahn, B.M., Litvinovsky, B.A., Zanvilevich, A.N., Reichow, M., 2009. Peralkaline granitoid
Wang, and Jianming Yang for discussions on this manuscript. Many of magmatism in the Mongolian-Transbaikalian Belt: Evolution, petrogenesis and tec-
tonic significance. Lithos 113, 521–539.
the ideas in this paper were initiated and rectified during these dis- Ji, J.S., Tao, H.X., Zeng, Z.R., Li, H.Q., Zhang, L.C., 1994. Geology of the Kanggurtag Gold
cussions. This study was financially supported by funds from the Mineralization Zone and Exploration. Geological Publishing House, East Tianshan,
National Key R&D Program of China (2017YFC0601206), the NSFC Beijing, pp. 136.
Kovalenko, V.I., Yarmolyuk, V.V., Kovach, V.P., Kotov, A.B., Kozakov, I.K., Salnikova,
Project (41772078, 40725009, 40421303, and 40572043), the State E.B., Larin, A.M., 2004. Isotope provinces, mechanisms of generation and sources of
Key Laboratory of Lithospheric Evolution, the Chinese State 973 Project the continental crust in the Central Asian mobile belt. Geological and isotopic evi-
(2001CB409801) and Hong Kong RGC (7066/07P). This paper is a dence. J. Asian Earth Sci. 23, 605–627.
contribution to the ILP (ERAS) and IGCP 480. Lamb, M.A., Badarch, G., Navratil, T., Poier, R., 2008. Structural and geochronologic datafrom the Shin Jinst area, eastern Gobi Altai, Mongolia: implications for Phanerozoic
intracontinental deformation in Asia. Tectonophysics 451, 312–330.
References Laurent-Charvet, S., Charvet, J., Monie, P., Shu, L., 2003. Late Paleozoic strike-slip shear
zones in eastern central Asia (NW China): new structural and geochronological data.
Tectonics 22, 1009.
Allen, M.B., Windley, B.F., Zhang, C., 1993. Palaeozoic collisional tectonics and mag- Liu, D.Q., Chen, Y.C., Wang, D.H., 2003. A discussion on problems related to miner-
matism of the Chinese Tien Shan, central Asia. Tectonophysics 220, 89–115. alisation of Tuwu-Yandong Cu-Mo ore field in Hami, Xinjiang. Min. Deposits 22,
Badarch, G., Cunningham, W.D., Windley, B.F., 2002. A new terrane subdivision for 334–344 (in Chinese with English abstract).
Mongolia: implications for the Phanerozoic crustal growth of Central Asia. J. Asian Li, W., Jackson, S.E., Pearson, N.J., Graham, S., 2010. Copper isotopic zonation in the
Earth Sci. 21, 87–110. Northparkes porphyry Cu-Au deposit, SE Australia. Geochim. Cosmochim. Acta 74,
Berzina, A.N., Sotnikov, V.I., Economou-Eliopoulos, M., Eliopoulos, D.G., 2005. 4078–4096.
Distribution of rhenium in molybdenite from porphyry Cu-Mo and Mo-Cu deposits of Li, X.H., Liu, Y., Li, Q.L., Guo, C.H., Chamberlain, K.R., 2009, Precise determination of
Russia (Siberia) and Mongolia. Ore Geol. Rev. 26, 91–113. Phanerozoic zircon Pb/Pb age by multi-collector SIMS without external standardi-
Chen, Y.J., Zhang, C., Wang, P., Franco, P., Li, N., 2017. The Mo deposits of Northeast zation. Geochem. Geophys. Geosyst. 10, Q04010. doi:10.1029/cGC002400.
China. A powerful indicator of tectonic settings and associated evolutionary trends. Ludwig, K.R., 2001, User’s manual for Isoplot/Ex (rev. 2.49). A geochronological toolkit
Ore Geol. Rev. 81, 602–640. for Microsoft Excel. Berkeley Geochronology Center Special Publication 1, 1–55.
Chen, B., Jahn, B.M., Tian, W., 2009. Evolution of the Solonker suture zone: constraints Ma, R.S., Shu, L.S., Sun, J., 1997. Tectonic Evolution and Metallogeny of Eastern
from zircon U-Pb ages, Hf isotopic ratios and whole-rock Nd–Sr isotope compositions Tianshan Mountains. Geological Publishing House, Beijing, pp. 202.
of subduction- and collision-related magmas and forearc sediments. J. Asian Earth Mao, J.W., Zhang, Z.H., Zhang, Z.C., Du, A.D., 1999. Re-Os isotopic dating of molybde-
Sci. 34, 245–257. nites in the XiaoliugouW(Mo) deposit in the Northern Qilian mountains and its
Coleman, R., 1989. Continental growth of Northwest China. Tectonics 8, 621–635. geological significance. Cheochimica et Cosmochimica Acta 63, 1815–1818.
Deng, F.Y., 2012. Magma rocks of geochemistry characteristics s of East Gobi mo- Mao, J.W., Yang, J.M., Qu, W.J., Du, A.D., Wang, Z.L., Han, C.M., 2002. Re-Os age of Cu-
lybdenum mine in Hami, Xinjiang. Western Explor. Eng. 3, 115–119 (in Chinese with Ni ores from the Huangshandong Cu-Ni sulfide deposit in the East Tianshan
English abstract). Mountains and its implication for geodynamic processes. Min. Deposits 21, 323–330
Deng, X.H., Wang, J.B., Pirajno, F., Wang, Y.W., Li, Y.C., Li, C., Zhou, L.M., Chen, Y.J., (in Chinese with English abstract).
2016. Re-Os dating of chalcopyrite from selected mineral deposits in the Kalatag Mao, J.W., Pirajno, F., Cook, N., 2011. Mesozoic metallogeny in East China and corre-
district in the eastern Tianshan Orogen, China. Ore Geol. Rev. 77, 72–81. sponding geodynamic settings-An introduction to the special issue. Ore Geol. Rev.
Deng, X.H., Chen, Y.J., Santosh, M., Wang, J.B., Li, C., Yue, S.W., Zheng, Z., Chen, H.J., 43, 1–7.
Tang, H.S., Dong, L.H., Qu, X., 2017. U-Pb zircon, Re-Os molybdenite geochronology Mao, J.W., Du, A.D., Seltmann, R., Yu, J.J., 2003. Re-Os ages for the Shameika porphyry
and Rb-Sr geochemistry from the Xiaobaishitou W (-Mo) deposit. implications for Mo deposit and the Lipovy Lograre metal pegmatite, central Urals, Russia. Minerlium
Triassic tectonic setting in eastern Tianshan,NW China. Ore Geol. Rev. 80, 332–351. Deposita 38, 251–257.
Delibaş, O., 2009, The role of magma mixing processes in the formation of iron, copper, Mao, J.W., Xie, G.Q., Zhang, Z.H., Li, X.F., Wang, Y.T., Zhang, C.Q., Li, Y.F., 2005.
molybdenum and lead mineralizations of Kırıkkale-Yozgat region (Ph. D. thesis). Mesozoic large-scale metallogenic pulses in North China and corresponding geody-
Hacettepe University, Turkey, p. 210. namic settings. Acta Petrologica Sinica 21, 169–188 (in Chinese with English ab-
Delibaş, O., Genc, Y., Decampos, C. P., 2011, Magma mixing and unmixing related mi- stract).
neralization in the Karacaali Magmatic Complex. In: Sial, A.N., Bettencourt, J.S., Mao, J.W., Wang, Y.T., Bernd, L., Yu, J.J., Du, A.D., Mei, Y., Li, Y.F., Zang, W., Stein, H.J.,
Decampos, C.P., Ferreira, V.P. (eds.), Granite-related ore deposits. Geological Society Zhou, T.F., 2006. Molybdenite Re-Os and albite 40Ar/39Ar dating of Cu-Au-Mo and
Special Publications, London, vol. 350, pp. 149–173. magnetite porphyry systems in the Yangtze River valley and metallogenic implica-
Ding, T.P., Valkiers, S., Wang, D.F., Bai, R.M., Zou, X.Q., Li, Y.H., Zhang, Q.L., De Bievre, tions. Ore Geol. Rev. 29, 307–324.
P., 2001. The δ32S and δ34S values and absolute 32S/33S and 32S/34S ratios of Markey, R., Stein, H., Morgan, J., 1998. Highly precise Re-Os dating for molybdenite
IAEA and Chinese sulfur isotope reference materials. Bull. Mineral. Petrol. Geochem. using alkaline fusion and NTIMS. Talanta 45, 935–946.
20, 425–427 (in Chinese with English abstract). Orolmaa, D., Erdenesaihan, G., Borisenko, A.S., Fedoseev, G.S., Babich, V.V., Zhmodik,
Du, A.D., He, H.L., Yin, N.W., 1995. A study of the rhenium-osmium geochronometry of S.M., 2008. Permian-Triassic granitoid magmatism and metallogeny of the Hangayn
molybdenites. Acta Geol. Sin. 8, 171–181 (in Chinese with English abstract). (central Mongolia). Russ. Geol. Geophys. 49, 534–544.
Du, A.D., Wang, S.X., Sun, W.D., Zhang, D., Liu, D., 2001, Precise Re-Os dating of mo- Seltmann, R., Porter, T.M., 2005, The porphyry Cu-Au/Mo deposits of Central Eurasia. 1.
lybdenite using Carius tube, NTIMS and ICPMS. In. Piestrzynski et al (eds.) Mineral Tectonic, geologic and metallogenic setting and significant deposits. In: Porter, T.M.
Deposits at the 21st Century, pp. 405–407. (ed.), Super Porphyry Copper and Gold Deposits. A Global Perspective. PGC
Gao, J., Klemd, R., Zhu, M.T., Li, J.L., Bo Wan, B., Xiao, W.J., Qingdong Zeng, Q.D., Shen, Publishing, Adelaide 2, pp. 467–512.
P., Sun, J.G., Qin, K.Z., Campose, E., 2018. Large-scale porphyry-type mineralization Seltmann, R., Mike Porter, T., Pirajno, F., 2014. Geodynamics and metallogeny of the
in the Central Asian metallogenic domain: A review. J. Asian Earth Sci. 165, 7–36. central Eurasian porphyry and related epithermal mineral systems. A review. J. Asian
Goldfarb, R.J., Taylor, R.D., Collins, G.S., Goryachev, N.A., Orlandini, O.F., 2013. Earth Sci. 79, 810–841.
Phanerozoic continental growth and gold metallogeny of Asia. Gondwana Res. 25, Şengör, A.M.C., Natal'in, B.A., Burtman, U.S., 1993. Evolution of the Altaid tectonic
48–102. collage and Paleozoic crustal growth in Eurasia. Nature 364, 209–304.
Guo, F., 2000. Affinity between Palaeozoic blocks of Xinjiang and their suturing ages. Şengör, A.M.C., Natal'in, B.A., 1996. Turkic-type orogeny and its role in the making of the
Acta Geol. Sin. 74, 1–6. continental crust. Annu. Rev. Earth Planet. Sci. 24, 263–337.
Han, C.M., Xiao, W.J., Zhao, G.C., Mao, J.W., Li, S.Z., Yan, Z., Mao, Q.G., 2006. Major Shirey, S.B., Walker, R.J., 1995. Carius tube digestion for low-bank rhenium-osmium
types, characteristics and geodynamic mechanism of Late Paleozoic copper deposits analysis. Anal. Chem. 67, 2136–2141.
in Northern Xinjiang, Northwestern China. Ore Geol. Rev. 28, 308–328. Smoliar, M.I., Warker, R.J., Morgan, J.W., 1996. Re-Os ages of group IIA, IIIA, IVA and
Han, C.M., Xiao, W.J., Zhao, G.C., Sun, M., Qu, W.J., Du, A.D., 2010. In-Situ U-Pb, Hf and VIB iron meteorites. Science 271, 1099–1102.
Re-Os isotopic analyses of the Xiangshan Ni-Cu-Co deposit in Eastern Tianshan Stacey, J.S., Kramers, J.D., 1975. Approximation of terrestrial lead isotope evolution by a
(Xinjiang), Central Asia Orogenic Belt. constraints on the timing and genesis of the two-stage model. Earth Planet. Sci. Lett. 26, 207–221.
mineralization. Lithos 120, 547–562. Stein, H.J., Markey, R.J., Morgan, J.W., Du, A.D., Sun, Y.L., 1997. Highly precise and
283
C. Han et al. Journal of Asian Earth Sciences 165 (2018) 270–284
accurate Re-Os ages for molybdenite from the East Qinling molybdenium belt, Wu, Y.S., Wang, P., Yang, Y.F., Xiang, N., Li, N., Zhou, K.F., 2014. Ore geology and fluid
Shaanxi Province, China. Econ. Geol. 92, 827–835. inclusion study of the the Donggebi giant porphyry Mo deposit, Eastern Tianshan,
Tu, L.Q., Ma, Y.F., Shi, S.R., Yin, J.F., Tu, J.F., 2011. Geological and wall-rock alteration NW China. Geol. J. 49, 559–573.
characteristics of the Donggebi deposit, Hami City. Xinjiang Geol. 29, 433–436 (in Xiao, W.J., Zhang, L.C., Qin, K.Z., Sun, S., Li, J.L., 2004a. Paleozoic accretionary and
Chinese with English abstract). collisional tectonics of the Eastern Tianshan (China). Implications for the continental
Ueda, A., Sakai, H., 1984. Sulfur isotope study of Quaternary volcanic rocks from the growth of central Asia. Am. J. Sci. 304, 370–395.
Japanese Islands arc. Geochim. Cosmochim. Acta 48, 1837–1848. Xiao, W.J., Windley, B.F., Hao, J., Zhai, M.G., 2003, Accretion leading to collision and the
Wang, Y., Sun, G., Li, J., 2010. U-Pb (SHRIMP) and 40Ar/39Ar geochronological con- Permian Solonker suture, Inner Mongolia, China. termination of the Central Asian
straints on the evolution of the Xingxingxia shear zone, NW China: a Triassic segment orogenic belt. Tectonics 22, 069, doi:10.1029/2002TC1484.
of the Altyn Tagh fault system. Geol. Soc. Am. Bull. 122, 487–505. Xiao, W.J., Windley, B.F., Badarch, G., Sun, S., Li, J.L., Qin, K.Z., Wang, Z.H., 2004b.
Wang, B., 2011. Geological characteristics and prospecting types of East Gobi mo- Palaeozoic accretionary and convergent tectonics of the southern Altaids. implica-
lybdenum mine in Hami. China Molybdenum Indust. 35, 7–10 (in Chinese with tions for the lateral growth of Central Asia. J. Geol. Soc., London 161, 339–342.
English abstract). Xiao, W., Windley, B.F., Hao, J., Zhai, M., 2003b. Accretion leading to collision and the
Wiedenbeck, M., Alle, P., Corfu, F., Griffin, W.L., Meier, M., Oberli, F., Vonquadt, A., Permian Solonker suture, Inner Mongolia, China. Termination of the central Asian
Roddick, J.C., Speigel, W., 1995. Three natural zircon standards for U-Th-Pb, Lu-Hf, orogenic belt. Tectonics 22 (6), 1–20.
trace element and REE analyses. Geostand. Newslett. 19, 1–23. Xiao, W., Kroner, A., Windley, B., 2009. Geodynamic evolution of Central Asia in the
Windley, B.F., Allen, M.B., Zhang, C., Zhao, Z.Y., Wang, G.R., 1990. Paleozoic accretion Paleozoic and Mesozoic. Int. J. Earth Sci. 98, 1185–1188.
and Cenozoic re-deformation of the Chinese Tien Shan Range, Central Asia. Geology Yarmolyuk, V.V., Kovalenko, V.I., Sal'nikova, E.B., Budnikov, S.V., Kovach, V.P., Kotov,
18, 128–131. A.B., Ponomarchuk, V.A., 2002. Tectono-Magmatic zoning, magma sources and
Windley, B.F., Alexeiev, D., Xiao, W.J., Kröner, A., Badarch, G., 2007. Tectonic models for geodynamics of the early Mesozoic Mongolia-Trasbaikal province. Geotectonics 36,
accretion of the Central Asian Orogenic Belt. J. Geol. Soc. 64, 31–47. 293–311.
Wu, F.Y., Jahn, B.M., Wilde, S., Sun, D.Y., 2000. Phanerozoic crustal growth. U-Pb and Sr- Yang, Z.Q., Wu, B.Y., Zheng, S.S., An, J.L., Chang, Y.Q., 2011. Geological and geo-
Nd isotopic evidence from the granites in northeastern China. Tectonophysics 328, chemistical characteristics of ore-forming granite porphyry in East Gobi porphyry
89–113. molybdenum deposit in Xinjiang. Geol. Min. Resources South China 27, 208–214 (in
Wu, F.Y., Sun, D.Y., Li, H., Jahn, B.-M., Wilde, S., 2002. A-type granites in northeastern Chinese with English abstract).
China. age and geochemical constraints on their petrogenesis. Chem. Geol. 187, Zhang, H.T., So, C.S., Yun, S.T., 1999. Regional geologic setting and metallogenesis of
143–173. central Inner Mongolia, China. Guides for exploration of mesothermal gold deposits.
Wu, F.Y., Yang, Y.H., Xie, L.W., Yang, J.H., Xu, P., 2006. Hf isotopic compositions of the Ore Geol. Rev. 14, 129–146.
standard zircons and baddeleyites used in U-Pb geochronology. Chem. Geol. 234, Zhang, L.C., Liu, T.B., Shen, Y.C., 2002. Isotopic geochronology of the Late Paleozoic
105–126. Kangguer gold deposits of East Tianshan Mountains, Xinjiang, NW China. Resour.
Wu, F.Y., Sun, D.Y., Ge, W.C., Zhang, Y.B., Grant, M.L., Wilde, S.A., Jahn, B.M., 2011. Geol. 52, 249–261.
Geochronology of the Phanerozoic granitoids in northeastern China. J. Asian Earth Zhang, L.C., Xiao, W.J., Qin, K.Z., Qu, W.J., Du, A.D., 2005a. Re-Os isotopic dating of
Sci. 41, 1–30. molybdenite and pyrite in the Baishan Mo-Re deposit, eastern Tianshan, NW China,
Wu, Y.S., Chen, Y.J., Zhou, K.F., 2017a. Mo deposits in Northwest China. Geology, geo- and its geological significance. Miner. Deposita 39, 960–969.
chemistry, geochronology and tectonic setting. Ore Geol. Rev. 81, 641–671. Zhang, Z.Z., Gu, L.X., Wu, C.Z., Li, W.Q., Xi, A.H., Wang, S., 2005b. Zircon SHRIMP dating
Wu, Y.S., Zhou, K.F., Li, N., Chen, Y.J., 2017b. Zircon U-Pb dating and Sr–Nd–Pb–Hf for the Weiya pluton, eastern Tianshan: its geological implications. Acta Geologica
isotopes of the ore-associated porphyry at the giant the Donggebi Mo deposit, Eastern Sinica (English Edition) 79, 481–490.
Tianshan, NW China. Ore Geol. Rev. 81, 794–807.
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