Journal of Asian Earth Sciences 79 (2014) 696–709

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Journal of Asian Earth Sciences

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Zircon U–Pb and molybdenite Re–Os dating of the Chalukou porphyryMo deposit in the northern Great Xing’an Range, China and its geologicalsignificance

1367-9120/$ - see front matter � 2013 Elsevier Ltd. All rights reserved.http://dx.doi.org/10.1016/j.jseaes.2013.06.020

⇑ Corresponding author. Tel.: +86 01068999050.E-mail address: junliu@yeah.net (J. Liu).

Jun Liu a,⇑, Jingwen Mao a, Guang Wu a, Feng Wang b, Dafeng Luo b, Yanqing Hu b

a MLR Key Laboratory of Metallogeny and Mineral Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences, Beijing 100037, Chinab Yunnan Chihong Zinc & Germanium Limited Liability Company, Qujing, Yunan 655011, China

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

Article history:Available online 20 July 2013

Keywords:Zircon LA-ICP-MS U–Pb datingMolybdenite Re–Os datingPorphyry Mo depositMesozoic magma rocksChalukouGreat Xing’an Range

The newly discovered Chalukou giant porphyry Mo deposit, located in the northern Great Xing’an Range,is the biggest Mo deposit in northeast China. The Chalukou Mo deposit occurs in an intermediate-acidcomplex and Jurassic volcano-sedimentary rocks, of which granite porphyry, quartz porphyry, andfine-grained granite are closely associated with Mo mineralization. However, the ages of the igneousrocks and Mo mineralization are poorly constrained. In this paper, we report precise in situ LA-ICP-MSzircon U–Pb dates for the monzogranite, granite porphyry, quartz porphyry, fine grained granite, rhyoliteporphyry, diorite porphyry, and andesite porphyry in the Chalukou deposit, corresponding with ages of162 ± 2 Ma, 149 ± 5 Ma, 148 ± 2 Ma, 148 ± 1 Ma, 137 ± 3 Ma, 133 ± 2 Ma, and 132 ± 2 Ma, respectively.Analyses of six molybdenite samples yielded a Re–Os isochron age of 148 ± 1 Ma. These data indicate thatthe sequence of the magmatic activity in the Chalukou deposit ranges from Jurassic volcano-sedimentaryrocks and monzogranite, through late Jurassic granite porphyry, quartz porphyry, and fine-grained gran-ite, to early Cretaceous rhyolite porphyry, diorite porphyry, and andesite porphyry. The Chalukou por-phyry Mo deposit was formed in the late Jurassic, and occurred in a transitional tectonic setting fromcompression to extension caused by subduction of the Paleo-Pacific oceanic plate.

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1. Introduction

The Great Xing’an Range area is located on the southern marginof the Siberia Plate, a region with strong superposition of the Paleo-zoic Paleoasian tectonic-metallogenic domain and the MesozoicWestern Pacific marginal tectonic-metallogenic domain. Mostdeposits found to date are closely associated with the Mesozoicmagmatic hydrothermal activity, and the deposit types are mainlyporphyry, skarn, hydrothermal veins, and epithermal deposits(Zhao and Zhang, 1997; Liu et al., 2004; Chen et al., 2007). TheMesozoic granite and volcanic rocks are widely distributed in theGreat Xing’an Range (Sengör and Natal’in, 1996). The degree ofexploration is relatively high in the southern segment of the GreatXing’an Range, with Pb–Zn, Ag, Cu, Sn, and rare earth element (REE)deposits. Several large mineral deposits have been discovered,including the Dajin polymetallic tin deposit (Chu et al., 2002),Huanggang Fe–Sn deposit (Zhou et al., 2010), Bairendaba Ag–Pb–Zn deposit (Liu et al., 2010a), and Baerzhe REE deposit (Niu et al.,2008). Large deposits discovered in the Manzhouli area of thenorthern segment include the Wunugetushan Cu–Mo deposit

(Qin et al., 1999; Li et al., 2007), Jiawula Ag–Pb–Zn deposit (Zhaiet al., 2010), Chaganbulagen Ag–Pb–Zn deposit (Wu et al., 2010),and Erentaolegai Ag–Mn deposit (Wu et al., 2010). Overall, a fewlarge or medium deposits have been discovered in the majorityof the northern segment, and the mineralization age of the Duo-baoshan porphyry Cu–Mo deposit discovered in the 1950s is EarlyPaleozoic (Liu et al., 2010b, 2012). The scale and number of depos-its found in the northern segment of the Great Xing’an Range arefar less than those of the southern segment. For a long time, thisarea was primarily exploited for hydrothermal vein-type Pb–Zn–Ag deposits and epithermal Au deposits. However, the discoveryof the Chalukou giant Mo deposit indicates that this area has astrong potential for porphyry molybdenum mineralization. TheChalukou porphyry Mo deposit was discovered in 2005, and the ex-plored industrial Mo resource is about 1.78 Mt with an averagegrade of 0.09%; the resource of marginal Mo ore is 0.68 Mt withan average grade of 0.05%; the Pb + Zn is about 0.37 Mt with anaverage grade of 1.27%; and the amount of associated Ag is about814 t with an average grade of 2 g/t (JMIC, 2010, 2011). Update,the Chalukou giant porphyry Mo deposit is the largest Mo depositin northeast China.

The current research of the Chalukou deposit is only limitedto descriptions of the geological features, such as scale,

J. Liu et al. / Journal of Asian Earth Sciences 79 (2014) 696–709 697

mineralization type, orebody morphology (Lü et al., 2010; Liu et al.,2011). Re–Os isotopic dating of eight molybdenite samples yieldedan isochron age of 147 Ma (Nie et al., 2011). The mineralization ofthe Chalukou Mo deposit is proposed to be related to an interme-diate-acid complex in the area, but there is a gap in the publishedresearch concerning the age of intrusive and subvolcanic rocks fordifferent periods. Based on observation and analysis of the rela-tionship between the orebodies of the Chalukou deposit and therelated porphyry and all types of wall-rocks, this study selectedintrusive and subvolcanic rocks of the Chalukou deposit for theLA-ICP-MS (Laser Ablation Multicollector inductively Coupled Plas-ma Mass Spectrometry) zircon U–Pb dating, and dated the relatedores with molybdenite Re–Os method so as to eliminate the rock-and ore-forming age framework and integrate the mineralizationwith its corresponding tectonic setting.

2. Geological setting

The Xing’an–Mongolia orogenic belt, which is east of the Paleo-asian or Central Asian orogenic belt and between the Siberia Cratonand the North China Craton, is composed of a series of micro-con-tinental blocks (Sengör et al., 1993; Jahn et al., 2000; Jahn, 2004; Li,2006; Wu et al., 2012). The Xing’an–Mongolia orogenic belt andthe southern North China Craton are separated by the Chifeng-Kaiyuan fault. The Tayuan-Xiguitu, Hegenshan-Heihe, and Jiamu-si-Mudanjiang faults separate the Xing’an–Mongolia orogenic beltfrom northwest to southeast into the Argun, Xing’an, Songliao, andJiamusi blocks (Wu et al., 2007)(Fig. 1a). Located mainly on theXing’an and Argun blocks, the Great Xing’an Range area is knownfor large outcropping Mesozoic granite and volcanic rocks (Fanet al., 2003; Ge et al., 2005a, 2007; Wang et al., 2006; Zhanget al., 2008) and is divided into southern and northern segmentswith the border at N47�200 (Zhao et al., 1989)(Fig. 1b).

During the Phanerozoic, northeastern China underwent a com-plex history, highlighted by multiple stages of accretion and colli-sion, although the time and manner of the amalgamation of the

Fig. 1. Geotectonic units (Fig. 1a after Zhang et al., 2010) and sketch regional geological mXing’an Range. F1, Tayuan-Xiguitu Fault; F2, Hegenshan-Heihe Fault; F3, Xilamulun-ChanFault; F7, Jiamusi-Mudanjiang Fault; , Chalukou Mo deposit; , Duobaoshan Cu–Mo d

micro-continents still remains controversial (Zhang et al., 2010).Studies on the Early Ordovician post-collisional granite and ophio-lite suite distributed along the Tayuan-Xiguitu fault suggest theXing’an block collided and merged with the Argun block alongthe Tayuan-Xiguitu fault in the Early Paleozoic (Yan et al., 1989;Zhang and Tang, 1989; Li, 1991; Ge et al., 2005b), and the Songliaoblock merged with the mentioned joint block along the Hegen-shan-Heihe fault in the Late Devonian-Early Carboniferous age(Hong et al., 1994; Chen et al., 2000; Sun et al., 2001; Wu et al.,2002; Zhou et al., 2005). In the Late Paleozoic, massive extensionactivity seems to have occurred in this area (Tang, 1990). In theEarly Mesozoic, the Jiamusi block merged with the composite blockinside the Xing’an–Mongolia orogenic belt along the Mudanjiangfault (Ge et al., 2005a, 2007).

The strata outcropped in the northern area of the Great Xing’anRange are mainly as metamorphic rocks in the PaleoproterozoicXinghuadukou Group, which constitutes the Precambrian crystal-line basement; shallow metamorphic rocks in the NeoproterozoicJiageda Group; the Cambrian, Ordovician, Silurian, Devonian, Car-boniferous, and Permian clastic and carbonate rocks in Paleozoiccover sequence; the Jurassic, Cretaceous volcaniclastic rocks anda coal-bearing seams. The intrusive rocks in the area were mainlyformed in the late Paleozoic and Mesozoic with a small amount inthe early Paleozoic. Early Paleozoic magmatic activity mainly oc-curred in the Mohe, Tahe, and Duobaoshan area of Nenjiang County(Ge et al., 2005b; Wu et al., 2005, 2012; Liu et al., 2012). Basic-ultrabasic rocks were mainly formed in the Late Paleozoic andmostly developed along the boundaries between the blocks. Mas-sive intermediate-acidic intrusive rocks were developed in the LatePaleozoic and Mesozoic (Liu et al., 2004). The Great Xing’an Rangearea was mainly affected by NS-trending compression between theSiberia Craton and the North China Craton prior to the EarlyJurassic, and it formed a series of fold belts and deep faults alongthe margin of two ancient continents that are mainly EW-trendingand then NE-trending. After the Mid-Late Jurassic, the maininfluence was the oblique subduction to northwest of the Pacific

ap (Fig. 1b after IMBGMR, 1991; HBGMR, 1993; SIGMR, 2005) of the northern Greatgchun Fault; F4, Chifeng-Kaiyuan Fault; F5, Dunhua-Mishan Fault; F6, Yilan-Yitong

eposit; , Tongshan Cu deposit; , Taipinggou Mo deposit.

698 J. Liu et al. / Journal of Asian Earth Sciences 79 (2014) 696–709

Plate toward the east of the Eurasian continent, which formed aseries of lattice fault systems with the coexistence of three faultsystems that exhibit NE-NNE-trending, EW-trending, and NW-trending, respectively.

3. Ore deposit geology

The Chalukou porphyry Mo deposit is located in the Zhuangzhiforest farm 80 km north of Jiagedaqi in the Great Xing’an Rangearea at geographic coordinates E123�4901500 to E123�5603000 andN51�0801500 to N51�1100000 (Fig. 1b). The deposit is divided intotwo exploration areas (Eastern River and Western River) borderingthe Duobukur River (Fig. 2). The degree of exploration is high in theEastern River area, and most of the Mo orebodies discovered up-date are concentrated in this area. Meanwhile, the degree of explo-ration in the Western River area is low, although it still shows agood Mo prospecting potential.

The rocks outcropped in the mining area are mainly metamor-phic rocks of the Neoproterozoic Dawangzi Formation and Jurassicvolcano-sedimentary rocks. The metamorphic rocks of the Daw-angzi Formation are mainly composed of metamorphic sandstone,silicalite, slate, phyllite, marble, and metavolcanic rocks. TheJurassic volcano-sedimentary rocks are mainly rhyolite, rhyolitictuff lava, dacite, trachyte, and andesite, which are important ore-bearing wall-rocks. The Cretaceous subvolcanic rocks are mainlyandesitic porphyry and rhyolite porphyry, and cut the early por-phyry rocks and Mo orebodies. The Intermediate-acidic intrusiverocks are relatively well developed, and the main rock types aremonzogranite, granite porphyry, quartz porphyry, fine-grainedgranite, and diorite rocks. The monzogranite rocks are mainly dis-tributed as batholiths or stocks. The granite porphyry rocks aremainly distributed as stocks ca. 600 m deep below the surfaceand the upper part appear as dykes and apophysis. Quartz por-phyry rocks are mainly emplaced as apophysis and dykes in theJurassic volcano-sedimentary rocks, mainly distributed below400 m at depth, and are produced in association with crypto-

Fig. 2. Regional geological sketch map of the Chalukou depo

explosive breccia (Figs. 3 and 4). The diorite dikes are no mineral-ized, and cut early granite porphyry, quartz porphyry, and orebod-ies controlled by late faults (Liu et al., 2011).

The tectonics mainly exhibit as two NE and NW-trend faults.The center of volcanic-magmatic activity was localized at the inter-section of these faults. Crypto-explosive breccia is relatively welldeveloped and is mainly distributed as tubular or lenticular bodies,or as pipes. The diameter of the breccia clasts is mostly less than10 cm, with individual clast reaching tens of centimeters. Mostbreccias are angular-subangular shaped and followed by sub-rounded varieties. The compositions of the breccias are mainlygranite porphyry, quartz porphyry, and monzogranite. The ce-ments are mainly rock fragments, hydrothermal siliceous cementand metallic sulfides, which contain molybdenite, pyrite, andchalcopyrite.

In the Chalukou deposit there developed two types of mineral-ization style: porphyry Mo mineralization and hydrothermalvein-type Pb–Zn–Ag mineralization. The overall Mo orebody isvault-like, as produced in granite porphyry, quartz porphyry,fine-grained granite, crypto-explosive breccia, and Jurassic vol-cano-sedimentary rocks. Deep Mo orebodies also occurred inmonzogranite. The Mo orebodies are mainly hidden with smallpart are exposed at the surface. The currently dominant Mo ore-body extends over 2600 m with a width of 360–1260 m and a ver-tical thickness generally of 200–900 m. The geometry of the Moorebodies is divided into three types, i.e., an upper thin-layeredorebody, a central thick-layered orebody, and a lower thicker-lay-ered orebody. The thin-layered orebodies appear as thin layers orveins with a small scale and poor continuity, and the thickness is7–55 m. The ore-bearing wall-rocks are mainly Jurassic volcano-sedimentary rocks with a small amount of quartz porphyry andan average Mo grade of 0.07–0.11%, grading downward to thethick-layered orebodies. The thick-layered orebodies appear asthick layers, or lenticular of large scale and good continuity witha total thickness of 51–148 m. The ore-bearing wall-rocks arequartz porphyry, granite porphyry, breccias, and Jurassic volcano-sedimentary rocks with an average Mo grade of 0.08–0.11%,

sit in northern Great Xing’an Range (JMIC, 2010, 2011).

Fig. 3. Simplified geologic map (a) and geological cross section along exploration line 10 in Eastern River area of the Chalukou deposit in northern Great Xing’an Range (b)(after Liu et al., 2011; Nie et al., 2011; JMIC, 2010, 2011).

Fig. 4. Geological cross section along exploration line 5 in Western River area (a) and exploration line 7 in Eastern River area (b) of the Chalukou deposit in northern GreatXing’an Range (after JMIC, 2010, 2011).

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grading downward to the thicker-layered orebodies. The thicker-layered orebodies appear as thick layers and thicker-layered oflarge scale and good continuity, and thickness is 112–349 m. the

ore-bearing wall-rocks are mainly granite porphyry, fine-grainedgranite, and intermediate-acidic volcanic and monzogranite withan average Mo grade of 0.09–0.11%. The Pb–Zn–Ag orebodies

Table 1Location of the intermediate-acid intrusions and subvolcanic rocks to date from theChalukou deposit.

No. SampleNo.

Rock type Explorationarea

Drillcore no.

Location ofsamples (m)

1 HD-243 Monzogranite EasternRiver

ZK1303 1393

2 HD-273 Graniteporphyry

EasternRiver

ZK903 861

3 HD-47 Quartzporphyry

EasternRiver

ZK901 1048

4 HX-9 Fine grainedgranite

WesternRiver

ZK5002 280

5 HD-105 Rhyoliteporphyry

EasternRiver

ZK1803 593

6 HD-212 Dioriteporphyry

EasternRiver

ZK1406 1467

7 HC-15 Andesiteporphyry

EasternRiver

ZK1803 903

700 J. Liu et al. / Journal of Asian Earth Sciences 79 (2014) 696–709

appear as veins and are mainly distributed in the upper part overthe Mo orebodies and are controlled by tectonic fracture zones,cracked zones, and alteration zones. The ore-bearing wall-rocksare mainly metamorphic rocks of the Dawangzi Formation orJurassic volcano-sedimentary rocks. There are more than 30 oreveins in the mine area. The orebodies are oriented from 30� to75� and inclined to the northwest at an inclination angle of 20�to 45�. The length is 100–3220 m, and the thickness is 1.5–3.6 m.The mineralization is zoned from the porphyry orebodies outwardand upward with zonings of Mo mineralization zone ? Mo–Pb–Zn–Ag mineralization zone ? Pb–Zn–Ag mineralization zone. Inthe Mo orebodies the ore distribution appears Mo-rich ore-body ? high and low-grade interbedded lenticular Mo ore-body ? low-grade thin-layered Mo orebody upward.

The Mo ores are mainly as stockwork, fine veins, massive, andbreccias. The Pb–Zn–Ag ores mainly occur as veins, fine veins, andmassive. The metallic minerals are mainly molybdenite, pyrite,sphalerite, and galena, accompanied by minor chalcopyrite, pyr-rhotite, magnetite, and hematite. The magnetite and hematiteare found in potassic alteration or granite porphyry. The gangueminerals are mainly quartz, K-feldspar, and plagioclase and minorfluorite, sericite, calcite, kaolinite, biotite, chlorite, and epidote.The molybdenite occurs as three main types: (1) as filling incracks of granite porphyry, quartz porphyry, monzogranite, Juras-sic volcano-sedimentary rocks, and metamorphic rocks of theDawangzi Formation as scales or films; (2) distributed withinquartz veins as disseminations or films in association with metal-lic sulfides, such as pyrite, chalcopyrite, and galena; and (3) dis-tributed as scattered granules in breccia cements in associationwith pyrite and chalcopyrite. The pyrite has three main occur-rences: (1) medium-coarse granules, lumps, or fine veins andcoexisting with a small amount of molybdenite and fluorite inquartz veins and altered granite; (2) distributed as medium-finegranules and hypidiomorphic-idiomorphic granules in varioustypes of altered rocks and quartz veins with a close relationshipwith Mo mineralization and Pb–Zn mineralization; and (3) dis-tributed as scattered granules and sparse disseminations in strataof the Dawangzi Formation and Jurassic volcano-sedimentaryrocks.

The alteration of wall-rocks is strong and zoning from thecenter of the porphyry body outward with potassic, sericitic,argillic, and propylitization zones. There are not any clearboundaries between mineralization zones, frequently showing agrading relationship. Except for potassic, sericitization, kaoliniti-zation, montmorillonitization, chloritization, epidotization, thereare silicification, fluoritization, carbonatization. The potassic,silicification, and fluoritizations are closely related to the Momineralization, whereas the fluoritization, silicification, andpropylitic alterations are closely related to the Pb–Zn–Agmineralization.

According to the mineral assemblages and ore fabrics, as well asthe cross-cutting relationships of veins, the mineralization processcan be preliminarily divided into three stages: early, middle, andlate. The early stage is a quartz + K-feldspar stage, and the mineralswere produced as quartz + K-feldspar veins, quartz + K-feld-spar + magnetite + hematite veins, and K-feldspar + magne-tite + hematite veins. The veins are mainly distributed deep inthe mine area. The second stage is a quartz + molybdenite stageincluding quartz ± fluorite + molybdenite veins, quartz ± fluo-rite + molybdenite + chalcopyrite + pyrite veins, and quartz + K-feldspar + molybdenite veins. The molybdenite is distributed asdisseminations or films in quartz veins. The last stage is aquartz + galena + sphalerite stage with quartz + pyrite veins,quartz ± carbonate + galena + sphalerite veins, quartz + fluo-rite + galena + sphalerite veins, fluorite + galena + sphalerite veins,and quartz + carbonate veins.

4. Sample characteristics

The samples used for the LA-ICP-MS zircon U–Pb dating in thiswork were fresh monzogranite, granite porphyry, quartz porphyry,fine-grained granite, rhyolite porphyry, diorite porphyry, andandesite porphyry from the Chalukou deposit. Fine-grained granitewas collected from the Western River area, and the other sampleswere all collected from the Eastern River area (Table 1; Figs. 3 and4a). The six molybdenite samples used for Re–Os dating were col-lected from quartz-K-feldspar-molybdenite veins; Mo mineralizedgranite porphyry, monzogranite and breccia (Table 2).

Monzogranite (HD-243): The rock has a granitic texture andmedium-grained texture, and is mainly composed of plagioclase(40%), K-feldspar (35%), quartz (20%), and biotite (5%). The plagio-clase appears as hypidiomorphic-idiomorphic boards, polysynthet-ic twins, and simple double-crystal growth with a size of 0.6–5 mmthat partly shows sericitization and epidotization. The K-feldsparappears as hypidiomorphic boards or xenomorphic granular,clathrate twins, and perthitic texture with a size of 0.8–4 mm,and is replaced by kaolinite. The quartz appears as hypidiomor-phic–xenomorphic granular, wavy extinction, and myrmekitic tex-ture with a size of 0.6–4 mm. Biotite appears as brown flakes witha size of 0.4–2 mm and is partly replaced by chlorite with iron sep-arated. The accessory minerals are zircon, titanite, and magnetite.

Granite porphyry (HD-273): The rock has a porphyritic texturewith approximately 10% phenocrysts that are mainly composed ofplagioclase (3%), K-feldspar (5%) and quartz (2%). The plagioclaseappears as hypidiomorphic boards, polysynthetic twins with a sizeof 0.3–2 mm that partly show sericitization. The K-feldspar ap-pears as hypidiomorphic boards or xenomorphic granular, perthitictexture with a size of 0.4–3 mm, and partly is replaced by kaolinite.The quartz appears as xenomorphic with a size of 0.3–3 mm. Thegroundmass has a micro-granular texture, and consists of K-feld-spar, plagioclase, and quartz with a size of <0.2 mm. The accessoryminerals are zircon and titanite.

Quartz porphyry (HD-47): The rock has a porphyritic texturewith approximately 10% phenocrysts that are mainly composedof quartz (6%), K-feldspar (3%), and plagioclase (1%). The quartz ap-pears as hypidiomorphic-xenomorphic granular, metasomatic tex-ture with a size of 0.6–4 mm. The K-feldspar appears ashypidiomorphic boards with a size of 0.6–2 mm and is replacedby kaolinite. The plagioclase appears as hypidiomorphic boards,polysynthetic twins with a size of 0.5–1.5 mm that partly showssericitization. The groundmass has a micro-granular texture, andconsists of micro-crystal feldspar and quartz with a size of<0.3 mm. The accessory minerals are zircon, apatite, and titanite.

Table 2Re–Os data of molybdenite from the Chalukou deposit.

No. SampleNo.

Location of sample Ores type Occurrence Re (ppm) 187Re (ppm) 187Os (ppb) Model age(Ma)

Measured 2r Measured 2r Measured 2r Measured 2r

1 HD-7 ZK1701 drill core1027m

Q-Kf-Mo vein Disseminated 2.5 0 1.6 0 3.8 0 145 2

2 HD-9 ZK1701 drill core984m

Q-Kf-Mo vein Disseminated 4.0 0 2.5 0 6.1 0.1 145 2

3 HD-231 ZK1406 drill core761m

Mo mineralized breccia Disseminated 23.5 0.2 14.8 0.1 35.9 0.3 146 2

4 HD-252 ZK503 drill core 821m Mo mineralized graniteporphyry

Veinlets 20.2 0.2 12.7 0.1 31.4 0.3 148 2

5 HC-54 ZK1303 drill core995m

Mo mineralized graniteporphyry

Veinlets 21.7 0.2 13.6 0.1 33.5 0.3 147 2

6 HD-55 ZK901 drill core 975m Mo mineralized monzogranite Films 9.6 0.1 6.0 0 14.8 0.1 148 2

Q, quartz; Kf, K-feldspar; Mo, molybdenite; 2r, standard error.

J. Liu et al. / Journal of Asian Earth Sciences 79 (2014) 696–709 701

Fine-grained granite (HX-9): The rock has a porphyritic-liketexture, and is mainly composed of quartz (45%), K-feldspar(40%), and plagioclase (15%). The quartz appears as hypidiomor-phic-xenomorphic granular, wave extinction with a size of 0.6–1.5 mm. The K-feldspar appears as hypidiomorphic-idiomorphicboards, clathrate twins, and perthitic texture with a size of 0.5–2 mm. A few of K-feldspars are replaced by kaolinite. The plagio-clase appears as hypidiomorphic boards, and polysynthetic twinswith a size of 0.4–1 mm. Biotite appears as brown hypidiomorphicflakes with a size of 0.2–0.5 mm. The accessory minerals are zirconand titanite.

Rhyolite porphyry (HD-105): The rock has a porphyritic texturewith approximately 5% phenocrysts that are mainly composed ofplagioclase (1%), K-feldspar (2%), and quartz (2%). The plagioclaseappears as hypidiomorphic boards, polysynthetic twins, and partlyshows sericitization with a size of 0.3–2 mm. K-feldspar appears ashypidiomorphic boards, clathrate twins with a size of 0.3–2.5 mm.The quartz appears as xenomorphic granular, metasomatic texturewith a size of 0.4–1.5 mm. The groundmass consists of cryptocrys-talline felsic minerals.

Diorite porphyry (HD-212): The rock has a porphyritic texturewith approximately 20% phenocrysts that are mainly composedof plagioclase (15%), amphibole (3%) and biotite (2%). The plagio-clase appears as hypidiomorphic-idiomorphic boards with a sizeof 1–10 mm and partly shows sericitization and silicification. Theamphibole appears as short columns with a size of 1–6 mm. Biotiteappears as brown hypidiomorphic-xenomorphic flakes with a sizeof 1–5 mm. The mineral composition of groundmass is similar tothose of phenocrysts with a size of 0.1–0.6 mm. The accessory min-erals are zircon and titanite.

Andesite porphyry (HC-15): The rock has a porphyritic texturewith approximately 15% phenocrysts that are mainly composedof plagioclase (10%), amphibole (2%) and biotite (3%). The plagio-clase appears as hypidiomorphic-idiomorphic boards, polysynthet-ic twins, and simple double-crystal growth with a size of 0.6–3 mmand partly shows sericitization and silicification. The amphiboleappears as short columns with a dark edge and a size of 0.3–2 mm. The center of the minor amphibole is replaced by quartz,chlorite, and epidote to appear as a pseudomorph. Biotite appearsas brown flakes with a size of 0.3–2 mm and is partly replaced bychlorite and epidote. The mineral composition of groundmass issimilar to those of phenocrysts with a size of <0.1 mm. Plagioclasein the groundmass is oriented as acicular crystallites, forming apilotaxitic texture, and there is a small amount of sericite andchlorite in the plagioclase microcrystalline gaps. The accessoryminerals are zircon and magnetite.

5. Analytical methods

5.1. LA-ICP-MS zircon U–Pb ages

Zircons were separated by heavy liquid and magnetic separa-tion methods at Chengxin Services Ltd., Langfang, China. Pure zir-cons were handpicked under a binocular microscope, thenmounted in epoxy resin and polished until the grain interiors wereexposed. The Cathodoluminescence (CL) images were obtainedusing a JSM6510 scanning electron microscope produced by JEOLCorporation (Japan) at the Beijing zircon dating navigation technol-ogy limited company. Zircon U–Pb dating was done by an Agilent7500a ICP–MS coupled with a Resonetics Resolution M-50 Laser-Ablation System at the State Key Laboratory of Isotope Geochemis-try of Guangzhou Institute of Geochemistry, Chinese Academy ofSciences, Guangzhou, China. Helium was used as a carrier gas totransport the ablated materials from the laser-ablation cell to theICP–MS torch. The NIST610 glass was used as an external standardto calculate U, Th, and Pb concentrations of unknowns (Pearceet al., 1997). The standard zircon TEMORA (Black et al., 2003)was used as an external standard to normalize isotopic fraction-ation during analysis. The diameter of the laser spot was 31 lmand frequency was 8 Hz. Analytical procedures used follow thosedescribed by Tu et al. (2011). Raw data were processed using theICPMSDataCal program (Version 6.7) (Liu et al., 2008). Uncertain-ties of individual analyses are reported with 1r errors; weightedmean ages were calculated at 1r confidence level. The data wereprocessed using the ISOPLOT (Ver 3.0) program (Ludwig, 2003).

5.2. Molybdenite Re–Os dating

Samples were crushed, separated, and sieved (roughly at firstand later more finely) to obtain monomineralic molybdenite witha purity >99%. The molybdenite crystal is fresh without oxidationand is not contaminated. The decomposition of the molybdenites,the pretreatment of the purification and separation of Re–Os andthe inductively coupled plasma–mass spectrometry (ICP–MS) anal-ysis of Re–Os content were conducted at the National ResearchCenter for Geoanalysis (Beijing). The chemical separation and massspectrometry of Re–Os consists of four steps: sample decomposi-tion, distillation separation of Os, extraction separation of Re andmass spectrometry. The analysis followed the procedures de-scribed by Du et al. (2004). The sample was dissolved in a sealedCarlos tube at 200 �C, Os was absorbed through distillation, andRe was extracted with acetone. The Re, 187Re and 187Os contentswere measured with the TJA PQ ExCell ICP–MS, manufactured by

702 J. Liu et al. / Journal of Asian Earth Sciences 79 (2014) 696–709

the TJA Company in the United States. Ordinary Os was computedby measuring the 192Os/190Os ratio based on the abundance of Osisotope with Nier value, and 187Os was the total 187Os isotope.For Re, we chose the mass numbers 185 and 187, and we moni-tored Os using 190; for Os, we chose the mass numbers 186, 187,188, 189, 190 and 192, and we monitored Re using 185. The uncer-tainty in the Re and Os content derives from the weighing error ofsamples and diluents, the calibration error of diluents, the fraction-ation correction error of mass spectrometry measurements and themeasurement error of isotope ratios in the analyzed samples; theconfidence level is 95%. Uncertainty in the model age derives fromuncertainty in the decay constant (1.02%); the confidence level is95%. The Re–Os model age is calculated as t = 1/k [ln(1 + 187Os/187Re], where k is the decay constant of 187Re, and theadopted value is k = 1.666 � 10�11/a (Smoliar et al., 1996). The po-sitive and negative isochron was computed with the ISOPLOT pro-gram (Ludwig, 2003).

6. Results

6.1. Zircon U–Pb ages

6.1.1. Monzogranite (HD-243)Zircon mostly appears as elongated columns, with a small por-

tion presenting short columns. The particle size is between 100 and250 lm. The zircons mostly are colorless, with a few yellowishbrown. The CL images indicate that most zircons possess cleargrowth zoning (Fig. 5a). The Th/U ratios of the 20 zircons are be-tween 0.43 and 0.98 with an average of 0.64 and greater than0.1. The Th content is between 41.4 ppm and 494.1 ppm with anaverage of 228.9 ppm. The U content is between 68.3 ppm and736.2 ppm with an average of 364.1 ppm. Therefore, zircon is ofmagmatic origin. In the 206Pb/238U–207Pb/235U concordia diagram(Fig. 6a), 19 analysis points for the 20 zircons are located on theconcordia and nearby, and the weighted average age of the206Pb/238U data is 162 ± 2 Ma (MSWD = 0.37). The concordia ageof the remaining one zircon is 205 ± 8 Ma (point HD-243.15), andit should be the captured early magmatic zircon.

6.1.2. Granite porphyry (HD-273)Zircon mostly appears as elongated columns, with a small por-

tion presenting short columns. Some zircons show an embayed orrounded edge. The particle size is concentrated between 100 and150 lm. The zircon crystals are colorless or yellowish brown. TheCL images indicate that most zircon crystals possess clear growthzoning, and the images of some zircons are relatively dark or rela-tively bright (Fig. 5b). Among the 16 analysis points for the 16 zir-cons, three (HD-273.09, HD-273.15, and HD-273.16) with anobvious dissonance are excluded. The Th/U ratios of the remaining13 zircon crystals are between 0.67 and 1.39 with an average of 1.0and greater than 0.1. The Th content is between 18.2 ppm and496.5 ppm with an average of 214.5 ppm. The U content is be-tween 24.4 ppm and 400.2 ppm with an average of 191.6 ppm.Therefore, zircon is assigned as being magmatic origin. The concor-dia ages of the two zircons are 165 ± 7 Ma and 174 ± 10 Ma (pointsHD-273.01 and HD-273.12), respectively; therefore, they should beearly magmatic zircon. In the 206Pb/238U–207Pb/235U concordia dia-gram (Fig. 6b), 11 analysis points are located on the concordia andnearby, and the weighted average age of the 206Pb/238U data is149 ± 5 Ma (MSWD = 3.1).

6.1.3. Quartz porphyry (HD-47)Zircon mostly appears as short columns, with a small portion

presenting elongated columns. The particle size is between 50and 100 lm. The zircons are colorless or shallow yellowish brown.

The CL images indicate that zircons show clear growth zoning(Fig. 5c). Among the 20 analysis points for the 20 zircons, one(HD-47.18) with an obvious dissonance are excluded. The Th/U ra-tios of the remaining 19 zircons are between 0.49 and 1.61 with anaverage of 1.1 and greater than 0.1. The Th content is between71.0 ppm and 527.2 ppm with an average of 294.7 ppm. The U con-tent is between 84.5 ppm and 468.1 ppm with an average of268.8 ppm. Therefore, zircon is assigned as being magmatic origin.In the 206Pb/238U–207Pb/235U concordia diagram (Fig. 6c), 19 analy-sis points are located on the concordia and nearby, and theweighted average age of the 206Pb/238U data is 148 ± 2 Ma(MSWD = 0.85).

6.1.4. Fine-grained granite (HX-9)Zircon mostly appears as short columns, with a small portion

presenting elongated columns. The particle size is concentrated be-tween 50 and 150 lm. The zircons mostly are yellowish brown,partly colorless. The CL images indicate that most zircons possessclear growth zoning, and the images of some zircon crystals are rel-atively dark (Fig. 5d). The Th/U ratios of the 20 zircons are between0.60 and 1.24 with an average of 0.9 and greater than 0.1. The Thcontent is between 89.5 ppm and 4009.3 ppm with an average of1943.7 ppm. The U content is between 139.1 ppm and4057.8 ppm with an average of 2197.7 ppm. Therefore, zircon is as-signed as being magmatic origin. In the 206Pb/238U–207Pb/235U con-cordia diagram (Fig. 6d), 20 analysis points are located on theconcordia and nearby, and the weighted average age of the206Pb/238U data is 148 ± 1 Ma (MSWD = 0.85).

6.1.5. Rhyolite porphyry (HD-105)Zircon mostly appears as elongated columns or short columns.

The particle size is between 50 and 100 lm. The zircons are color-less. The CL images indicate that most zircons possess clear growthzoning (Fig. 5e). Among the 20 analysis points for the 20 zircons,four (HD-105.09, HD-105.11, HD-105.13 and HD-105.17) with anobvious dissonance are excluded. The Th/U ratios of the remaining16 zircons are between 0.70 and 1.32 with an average of 1.0 andgreater than 0.1. The Th content is between 69.5 ppm and628.5 ppm with an average of 175.4 ppm. The U content is be-tween 83.0 ppm and 499.0 ppm with an average of 166.5 ppm.Therefore, zircons are assigned as being magmatic origin. The con-cordia age of the one zircon is 162 ± 7 Ma (points HD-105.12);therefore, it should be the captured early magmatic zircon. In the206Pb/238U–207Pb/235U concordia diagram (Fig. 6e), 15 analysispoints are located on the concordia and nearby, and the weightedaverage age of the 206Pb/238U data is 137 ± 3 Ma (MSWD = 2.0).

6.1.6. Diorite porphyry (HD-212)Zircon mostly appears as short columns, with a small portion

presenting elongated columns. The particle size is concentrated be-tween 50 and 100 lm. The zircon crystals mostly are colorless andpartly yellowish brown. The CL images indicate that most zirconcrystals possess clear growth zoning (Fig. 5f). Among the 20 anal-ysis points for the 20 zircon crystals, one (HD-212.16) with anobvious dissonance are excluded. The Th/U ratios of the remaining19 zircons are between 0.78 and 1.7 with an average of 1.1 andgreater than 0.1. The Th content is between 72.3 ppm and532.6 ppm with an average of 183.4 ppm. The U content is be-tween 81.3 ppm and 415.0 ppm with an average of 158.7 ppm.Therefore, zircons are assigned as being magmatic origin. In the206Pb/238U–207Pb/235U concordia diagram (Fig. 6f), 19 analysispoints are located on the concordia and nearby, and the weightedaverage age of the 206Pb/238U data is 133 ± 2 Ma (MSWD = 0.68).

Fig. 5. Representative cathodoluminescence (CL) images of zircons from the different intrusions and subvolcanic rock with analytical numbers of the Chalukou deposit innorthern Great Xing’an Range. (a) monzogranite; (b) granite porphyry; (c) quartz porphyry; (d) fine-grained granite; (e) rhyolite porphyry; (f) diorite porphyry; (g) andesiteporphyry.

J. Liu et al. / Journal of Asian Earth Sciences 79 (2014) 696–709 703

6.1.7. Andesite porphyry (HC-15)Zircon mostly appears as elongated columns or short columns.

The particle size is mainly between 50 and 100 lm. The zirconsare colorless. The CL images indicate that most zircons possessclear growth zoning (Fig. 5g). Among the 20 analysis points forthe 20 zircons, two (HC-15.03, HC-15.11) with an obviousdissonance are excluded. The Th/U ratios of the remaining 18zircons are between 0.79 and 1.50 with an average of 1.1 andgreater than 0.1. The Th content is between 81.1 ppm and

618.9 ppm with an average of 200.2 ppm. The U content is be-tween 82.4 ppm and 413.8 ppm with an average of 179.7 ppm.Therefore, the zircons are assigned as magmatic. The concordiaages of two zircons are 141 ± 4 Ma and 140 ± 4 Ma (points HD-105.08 and HD-105.19), respectively; therefore, they should beearly magmatic zircon. In the 206Pb/238U–207Pb/235U concordia dia-gram (Fig. 6g), 16 analysis points are located on the concordia andnearby, and the weighted average age of the 206Pb/238U data is132 ± 2 Ma (MSWD = 0.9).

Fig. 6. Zircon U–Pb concordia diagrams of the different intrusions and subvolcanic rock from the Chalukou deposit in northern Great Xing’an Range. (a) monzogranite; (b)granite porphyry; (c) quartz porphyry; (d) fine-grained granite; (e) rhyolite porphyry; (f) diorite porphyry; (g) andesite porphyry.

704 J. Liu et al. / Journal of Asian Earth Sciences 79 (2014) 696–709

6.2. Molybdenite Re–Os ages

The Re–Os isotope results of the 6 molybdenite samples areshown in Table 2. The Re content of molybdenite is between

2.5 ppm and 23.5 ppm with average of 13.6 ppm. The Re–Os modelage of six molybdenite samples is within a range of 145 ± 2 Ma to148 ± 2 Ma. We used ISOPLOT software to calculate the isochronfor the six data points, and we derived the isochron age of

Fig. 7. Re–Os isochron age of molybdenites from the Chalukou Mo deposit.

J. Liu et al. / Journal of Asian Earth Sciences 79 (2014) 696–709 705

148 ± 1 Ma (2r), with the initial 187Os of �0.084 ± 0.052 andMSWD = 1.7 (Fig. 7). The isochron age represents the time ofmolybdenite crystallization, namely, the mineralization age ofthe Chalukou Mo deposit is 148 ± 1 Ma.

7. Discussion

7.1. Ages of magmatism and mineralization

For the evolutionary sequence of magmatic rocks in the Chal-ukou deposit, the first concern is the intrusive age and order of mag-matic rocks. The area of the Middle Jurassic monzograniteoutcropped is relatively large in the Chalukou deposit. The graniteporphyry and quartz porphyry in the Eastern River area and thefine-grained granite in the Western River area are consistent inage, and all belong to the Late Jurassic hypabyssal intrusive rocks.The Re–Os isochron age of the molybdenite from the Chalukou de-posit is 148 ± 1 Ma, which is consistent with the intrusive time ofthe quartz porphyry, granite porphyry, and fine-grained granite.The ages of the andesite porphyry and diorite porphyry are consis-tent and are in good agreement (within the error range) with theage of the rhyolite porphyry as the Early Cretaceous hypabyssal-subvolcanic rock series. Although the exact age of this set of vol-cano-sedimentary rocks cannot be confirmed at present, it shouldbe the product of pre-mineralization volcanic activity. The orderof magmatic activity in the Chalukou deposit is the Jurassic vol-cano-sedimentary rocks, monzogranite ? the Late Jurassic graniteporphyry, quartz porphyry, fine-grained granite ? the Early Creta-ceous rhyolite porphyry, diorite porphyry, and andesite porphyry.According to the LA-ICP-MS zircon U–Pb dating results, the agesof the intrusive and volcanic rocks in the Chalukou deposit areranged between 132 ± 2 and 162 ± 2 Ma, while the magma-hydro-thermal activity at 148 ± 1 and 149 ± 5 Ma is closely related to thelarge-scale Mo–Pb–Zn–Ag mineralization of the Chalukou deposit.

The intrusive rocks were developed in at least three periods andinclude the Middle Jurassic monzogranite, Late Jurassic graniteporphyry, fine-grained granite and quartz porphyry, and EarlyCretaceous diorite porphyry. The Late Jurassic magmatic-hydro-thermal activity is temporally associated with large-scale Momineralization. The Middle Jurassic monzogranite is widelyexposed as the product of the early magmatic activities and theEarly Cretaceous diorite porphyry is post-mineralization and over-prints on the orebodies. The large-scale Mo mineralization in theEastern River area has a close relationship with granite porphyryand quartz porphyry, and the rocks with Mo mineralization found

in the Western River area are fine-grained granite. The zircon U–Pbage of these rocks is consistent, suggesting they are the products ofco-magmatic activity at the same period. At present, the degree ofexploration is high in the Eastern River area, which contains themajority of total Mo resources. Only a small amount of shallowdrilling was carried out in the Western River area. Therefore, wecannot exclude the possibility that more Mo resource will be dis-covered by further exploration. The zircon U–Pb ages of the andes-ite porphyry and rhyolite porphyry in the mining area are132 ± 2 Ma and 137 ± 3 Ma, respectively, belonging to the EarlyCretaceous, and they are post-mineralization subvolcanic rocks.The ages of the andesite porphyry and diorite porphyry are consis-tent and are the product of the magmatic activity of the same per-iod at different stages of evolution. Field observations indicate thatthe early Cretaceous rhyolite porphyry, andesite porphyry, anddiorite porphyry do contain Mo mineralization even cuttingthrough the Mo orebodies and porphyry rocks.

The porphyry deposits in northeastern China are distributed inthe overlapped region of the Central Asian Paleozoic metallogenicdomain and the West Pacific Mesozoic metallogenic domain. Thedeposits are mainly located inside the margin of intermediate-acidic intrusive-volcanic zones and are jointly controlled by NEand NW-trend faults. The Early Paleozoic Cu–Mo mineralizationis located in the Duobaoshan area where there are the Duobaoshanand Tongshan porphyry Cu–Mo deposits (Wu et al., 2009; Liu et al.,2010b, 2012). The Early-Middle Jurassic porphyry deposits, com-prising Wunugetushan Cu–Mo, Daheishan Mo, Lanjiagou Mo, andLianhuashan Cu deposits, developed between 160 and 190 Ma intime (Li et al., 2007; Dai et al., 2008; Wang et al., 2009). The EarlyCretaceous mainly developed porphyry Cu–Au mineralization of100 and 110 Ma, which is distributed on the margin of the Jiamusiblock, including the Xiaoxinancha Cu–Au and Tuanjiegou Au de-posits (Wang et al., 2004; Sun et al., 2008a). The discovery of theChalukou giant porphyry Mo deposit indicates that the Late Juras-sic was another important Mo mineralization period in northeastChina. The Re–Os age of the molybdenite from the Taipinggoumedium-sized porphyry Mo deposit recently discovered in north-ern Great Xing’an range is 129 Ma (Zhai et al., 2009), indicatingthat the Late Jurassic-Early Cretaceous was the important outbreakperiod of the Mo mineralization in the Great Xing’an Range area.

7.2. Geodynamic setting

There is significant controversy over the tectonic setting of theMesozoic magmatic activity in the Great Xing’an Range area. Threemain models have been proposed: (1) the plume model (Denget al., 1996; Lin et al., 1998; Ge et al., 1999; Shao et al., 2001);(2) the Mongolia–Okhotsk ocean closure and post-collisional oro-genesis model (Zorin, 1999; Fan et al., 2003; Meng, 2003; Chenet al., 2006; Ying et al., 2010); and (3) the Pacific Plate subductionmodel (Zhao et al., 1989; Wang et al., 2006; Zhang et al., 2008,2010). Wu et al. (2011) suggested that the Jurassic granite in north-eastern China is most likely associated with the subduction of thePacific Plate, the contemporary granite in the Argun block is relatedto the subduction and closure of the Mongolia–Okhotsk Ocean, andthe Jurassic granite in the Great Xing’an Range area is most likelyrelated to the collision and merging of the micro-blocks in the Xin-g’an–Mongolia orogenic belt.

The Mesozoic volcanic activity in the Great Xing’an Range areawas sustained for at least 40 Ma (Ying et al., 2010; Zhang et al.,2010). The volcanic rocks are mainly intermediate, there is a lackof basic-ultrabasic rocks, such as basalt, and there is no ring-shapedvolcanic belt (Ying et al., 2010; Sun et al., 2011). It is difficult to ex-plain such a temporal and spatial distribution of volcanic rocks inthe Great Xing’an Range with the plume model. The Mongolia–Okh-otsk Ocean was closed in the Middle Jurassic (Kravchinsky et al.,

706 J. Liu et al. / Journal of Asian Earth Sciences 79 (2014) 696–709

2002; Tomurtogoo et al., 2005) and had a limited influence on theGreat Xing’an Range area. It is possible that only the Mesozoic tec-tonic-magmatic activity in certain regions of the Argun block is re-lated to the evolution of the Mongolia–Okhotsk Ocean (Sun et al.,2011; Wu et al., 2011). A greater body of research data indicatesthat the Mesozoic magmatic activity in the Great Xing’an Rangehas a close relationship with the subduction of the Paleo-PacificPlate toward the Eurasian continent (Isozaki, 1997; Maruyama,1997; Huang and Zhao, 2006; Wu et al., 2007; Sui et al., 2007; Zhouet al., 2009; Zhang et al., 2010). Research on the accretionary com-plex rocks in northeastern China (Kojima,1987; Natal’in, 1993; Iso-zaki, 1997; Maruyama, 1997; Wu et al., 2007) and the structure ofthe lithosphere (Fukao et al., 1992; Huang and Zhao, 2006) confirmsthat eastern China has been located on the Paleo-Pacific subductionplate at least since the Mid-Late Jurassic, and the Qin-Hang Mid-Late Jurassic porphyry-skarn Cu–Mo and Pb–Zn–Ag deposits andrelated granitoids in South China (Mao et al., 2007, 2008a,2011a,d, 2013) represent the start of the subduction of the Paleo-Pacific subduction plate. In the past ten years more researching re-sults explained that the subduction of Paleo-Pacific plate played akey role in the tectonic movement and magmatic activity and met-allogeny in eastern China (Wu et al., 2003; Sun et al., 2005; Zhouet al., 2006; Li and Li, 2007; Sun et al., 2007, 2008b; Mao et al.,2002, 2003, 2004, 2005, 2006, 2007, 2008a,b,c, 2011a,b,c,d; Linget al., 2009). Research on the ophiolitic melange in the HeilongjiangGroup indicates that there was accretion and high-pressure meta-morphism on the southeast margin of the Early Jurassic Jiamusiblock, which represents the beginning of the Paleo-Pacific tectonicdomain (Sun et al., 2005; Wu et al., 2007; Zhou et al., 2009). Geo-physical data indicate the residual of an early subduction slab at adepth of 660 km in eastern China (Van der Voo et al., 1999; Huangand Zhao, 2006). Northeast Great Xing’an Range and Little Xing’anRange-Zhangguangcai Range have the same Jurassic granite distri-bution, which is similar to the granite composition on the marginsof active continents (Sui et al., 2007).

The volcanic rocks in the Great Xing’an Range area mainlyformed in the Late Jurassic-Early Cretaceous and peaked in theEarly Cretaceous (Ge et al., 2001; Chen et al., 2006; Wang et al.,2006; Zhang et al., 2008, 2010). The granite rocks in the Great Xin-g’an Range mainly formed in the Early Cretaceous, with a smallamount in the Jurassic (Jahn et al., 2001; Wu et al., 2002, 2003;Lin et al., 2004; Ge et al., 2007; Sui et al., 2007; Wu et al., 2011).The Early Cretaceous magmatic activity in the Great Xing’an Rangearea occurred in an extension setting (Ge et al., 2001; Guo et al.,2001; Fan et al., 2003; Gao et al., 2005; Zhang et al., 2008, 2010).

In the Jurassic, the subduction of the Paleo-Pacific Plate towardthe Eurasian Plate caused the crust to shorten and thicken. Thiscompression process reached the maximum in the Late Jurassic.Later, the subduction direction changed to north or northwest(Maruyama et al., 1997; Sagong et al., 2005; Zhang et al., 2010),causing the subduction-slipping of the Paleo-Pacific Plate (Chenget al., 2006). The change in the subduction direction of the Paleo-Pacific Plate (Zhang et al., 2010) or the break-off of subductionslabs (Wu et al., 2011) may result in the tectonic regime transitionfrom compression to extension in northeast China, causing large-scale delamination of the thickened continental crust and upwell-ing of the asthenosphere. The thinning of the lithosphere and theupwelling of asthenospheric material during this process causedstrong crust-mantle interaction. Underplating of the mantle-de-rived magma and the direct heating effect of the asthenosphereon the crust mixed with part of the overlying pre-existing crustalmaterial to form Mo-rich granitic magma. When the magmainvaded the shallow crust along weak tectonic zones, the rapidcooling and crystallization formed ore-bearing porphyry andlarge-scale Mo mineralization in the Chalukou area.

The large-scale mineralization in eastern China was concen-trated in three peak periods of 200–160 Ma, 140 Ma, and 120 Ma,corresponding to three geodynamic settings: post-collisionalorogenic processes, late in the great tectonic transition, andlarge-scale lithospheric thinning (Mao et al., 2003, 2005). The LateJurassic-Early Cretaceous tectonic transition in the Great Xing’anRange area is associated with the subduction direction change ofthe Paleo-Pacific Plate toward the Eurasian Plate and is consistentwith the transition of the compression–extension tectonic regimein eastern China. The mineralization age of the Chalukou depositis Late Jurassic, and the mineralization occurred during the transi-tion from compressional to extensional geodynamic setting causedby the subduction of the Paleo-Pacific Plate, which corresponded tothe formation of large-scale Mo mineralization in eastern China.

8. Conclusions

(1) The zircon U–Pb ages of the monzogranite, granite porphyry,quartz porphyry, fine grained granite, rhyolite porphyry,diorite porphyry and andesite porphyry are 162 ± 2 Ma,149 ± 5 Ma, 148 ± 2 Ma, 148 ± 1 Ma, 137 ± 3 Ma, 133 ± 2 Maand 132 ± 2 Ma, respectively. The order of magmatic activityin the Chalukou deposit is Jurassic volcano-sedimentaryrocks, monzogranite ? Late Jurassic granite porphyry,quartz porphyry, fine-grained granite ? Early Cretaceousrhyolite porphyry, diorite porphyry, and andesite porphyryconsistent with crosscutting relationships and texturalobservations.

(2) The Chalukou deposit is a classic porphyry Mo deposit,formed at 148 Ma. The Mo mineralization has a closerelationship with granite porphyry, quartz porphyry andfine-grained granite. The Middle Jurassic monzogranite ispre-mineralization intrusion whereas the Early Cretaceousmagmatic rocks are post-mineralization which overprintsthe porphyry Mo orebodies.

(3) The Chalukou deposit formed at the transitional tectonicsetting from compressional to extensional caused bysubduction of the Paleo-Pacific oceanic plate.

Acknowledgments

This study was supported by the National Science Foundation ofChina (Nos. 41202058, 41172081), Research Program of the Yun-nan Chihong Zinc & Germanium Limted Liability Company (No.201107ZKJS-01) and National Survey of Land and Resources (Nos.1212011085260, 12120113093600). We are grateful to Mr. MaojinCui, Youde Jin and Jianhua Zhang of the Yunnan Chihong Zinc &Germanium Limted Liability Company, and other geologists fromthe No. 706 Nonferrous Metal Geological Part of Heilongjiang Prov-ince for their helps during the field investigations. We also wouldlike to thank Mr. Xianglin Tu (a senior geologist), Ph. D CandidatesChongying Li and Saijun Sun concerning the LA-ICP-MS zircon U–Pb dating process at the Geochemistry of Guangzhou Institute ofGeochemistry, Chinese Academy of Sciences for the assistancesduring our laboratory work. Prof. Yitian Wang and Mr. Kejun Houare especially thanked for their constructive discussions and sug-gestions on earlier drafts of this paper.

Appendix A. Supplementary data

Supplementary data associated with this article can be found, inthe online version, at http://dx.doi.org/10.1016/j.jseaes.2013.06.020.

J. Liu et al. / Journal of Asian Earth Sciences 79 (2014) 696–709 707

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