Two Geodynamic–Metallogenic Events in the Balkhash (Kazakhstan) And

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International Geology Review, 2013 Vol. 55, No. 13, 1660–1687, http://dx.doi.org/10.1080/00206814.2013.792500

Two geodynamic–metallogenic events in the Balkhash (Kazakhstan) and the West Junggar (China): Carboniferous porphyry Cu and Permian greisen W-Mo mineralization Ping Shena*, Hongdi Panb , Wenjiao Xiaoa , Xuanhua Chenc , Seitmuratova Eleonoradd and Yuanchao Shena aKey Laboratory of Mineral Resources, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China; bCollege of Earth Sciences, Chang’an University, Xi’an 710054, China; cInstitute of Geomechanics, Chinese Academy of Geological Sciences, Beijing 100081, China; dLaboratory of Geological Formations, K. Satpaev Institute of Geological Sciences, Almaty 050010, Kazakhstan (Accepted 1 April 2013)

This study focuses on the geochronology and elemental and Nd isotopic geochemistry of the Baogutu Cu deposit and the newly discovered Suyunhe W-Mo deposit in the southern West Junggar ore belt (Xinjiang, China), as well as the geology of the newly discovered Hongyuan Mo deposit in the southern West Junggar ore belt and the Kounrad, Borly, and Aktogai Cu deposits and the East Kounrad, Zhanet, and Akshatau W-Mo deposits in the North Balkhash ore belt (Kazakhstan). The aim is to compare their petrogenesis, tectonic setting, and mineralization and to determine the relationship between the southern West Junggar and North Balkhash ore belts. Based on our newly acquired results, we propose that the Kounrad, Borly, Aktogai, and Baogutu deposits are typical porphyry Cu deposits associated with calc-alkaline magmas and formed in a Carboniferous (327–312 Ma) subduction-related setting. In contrast, the East Kounrad, Zhanet, Akshatau, Suyunhe, and Hongyuan deposits are quartz-vein greisen or greisen W-Mo or Mo deposits associated with alkaline magmas and formed in an early Permian (289–306 Ma) collision-related setting. Therefore, two geodynamic–metallogenic events can be distinguished in the southern West Junggar and North Balkhash ore belts: (1) Carboniferous subduction-related calc-alkaline magma – a porphyry Cu metallogenic event – and (2) early Permian collision-related alkaline magma – a greisen W-Mo metallogenic event. The North Balkhash ore belt is part of the Kazakhstan metallogenic zone, which can be extended eastward to the southern West Junggar in China. Keywords: Porphyry Cu deposits; greisen W-Mo deposits; Balkhash; Kazakhstan; West Junggar; China

1. Introduction begins at the Mointy block in the west and extends east- The Central Asian Orogenic Belt (CAOB) is the largest wards via Sayak to Aktogai in Kazakhstan (Figure 1B). The Phanerozoic juvenile crustal growth orogenic belt in the belt includes the Kounrad, Aktogai, and Borly porphyry Cu world, extending 7000 km from west to east and from the deposits and East Kounrad, Zhanet, and Akshatau greisen Siberian Craton in the north to the Tarim Craton in the W-Mo deposits, amongst which are both the Kounrad (with > > south (Figure 1A; Sengör et al. 1993; Xiao et al. 2009). The Cu reserves 8 Mt) and Aktogai (Cu 12 Mt), two late Palaeozoic tectonics of the CAOB was characterized world-famous super-large porphyry Cu deposits. However, by continuous subduction, accretion, and collision of vari- the relationship between these deposits has not been given ous micro-continental blocks during the formation, evolu- much attention, and whether the belt could be extended to tion, and closure of the Palaeo-Asian Ocean between the the West Junggar in China has not been discussed. The West Junggar metallogenic belt is bounded by

Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 Siberian and Tarim cratons (Xiao et al. 2008, 2009; Chen et al. 2010a). It led to the formation of a number of giant the Altai orogen to the north and by the Ashanti oro- ore deposits, which formed the Central Asian metallogenic gen to the south, and extends westward to the Balkhash domain (He and Zhu 2006;Zhuet al. 2007). The porphyry region in adjacent Kazakhstan and eastward to the Junggar Cu and greisen W-Mo deposits are particularly important Basin in Xinjiang, China (Figure 1B). This metallogenic in the Central Asian metallogenic domain. belt includes north and south zones, and in this study, The Balkhash metallogenic belt is world famous for we focused on the south zone (Figure 2). The southern its giant ore deposits. This metallogenic belt consists of West Junggar ore belt is famous for its gold deposits north and south zones. In this study, we study the north and nearly one hundred gold deposits of various sizes zone (i.e. the North Balkhash metallogenic belt). The belt have already been discovered, amongst which is the Hatu

*Corresponding author. Email: [email protected]

Figure 1. (A) Simplified map of the Central Asia Orogenic Belt (after Xiao et al. 2009). (B) Simplified geotectonic map of the Palaeozoic of Kazakhstan and contiguous China, showing major ore deposits (modified after Abdulin et al. 1996;Heet al. 2004; Windley et al. 2007; Xiao et al. 2008 and other sources). The Central Kazakhstan oroclinal bend is reflected by the inward younging of major magmatic arcs towards Lake Balkash. Note: Cm, Cambrian; O, Ordovician; S, Silurian; D, Devonian; C, Carboniferous; P, Permian; PZ, Palaeozoic; MZ, Mesozoic; CZ, Cenozoic. Subscripts 1, 2, and 3 refer to early, middle, and late.

(with Au > 50 t), one of the largest gold deposits in Mo deposits in the Kelamay Region and the Suyunhe Xinjiang. Recently, its ore potential has been highlighted by W-Mo deposit in the Barluk Mountains (Figure 2). Thus, the discovery of the Baogutu porphyry Cu and Hongyuan the southern West Junggar ore belt includes the porphyry 1662 P.Shen et al.

Figure 2. Generalized geological map of the West Junggar Region (modiﬁed after BGMRXUAR 1993;Shenet al. 2012a).

Cu, quartz vein W-Mo, and Mo deposits and considerable 2. Geological setting hydrothermal gold deposits. Therefore, it is possible that 2.1. West Junggar the southern West Junggar ore belt in China may be corre- The West Junggar terrain is largely composed of Palaeozoic lated with the North Balkhash ore belt in Kazakhstan. It is volcanic arcs in the northern part and accretionary com- necessary to study and compare the petrogenesis and tec- plexes in the southern (e.g. Windley et al. 2007; Xiao tonic setting as well as the mineralization types and ages et al. 2008; Zhang et al. 2011) that were accreted onto the in both the North Balkhash and southern West Junggar ore

Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 Kazakhstan plate as the Tarim, Kazakhstan, and Siberian belts in order to identify the extent of the North Balkhash plates converged (Chen and Arakawa 2005;Xiaoet al. ore belt in Xinjiang, China. 2008). In this work, we study the Kounrad, Borly, and Aktogai The southern West Junggar is located between latitudes Cu deposits and the East Kounrad, Zhanet, and Akshatau 45◦05 and 46◦15 N and longitudes 82◦15 and 86◦00 E W-Mo deposits in the North Balkhash (Kazakhstan), the (Figure 2). It is characterized by northeast-trending faults Baogutu Cu deposit and newly discovered Suyunhe W-Mo and fault-bounded accretionary complexes, which is in and Hongyuan Mo deposits in southern West Junggar contrast to the northern West Junggar where major faults (China), and also present new chemical and Nd isotopic and fault-bounded blocks are mainly EW oriented (Shen data and Re-Os isotopic ages for the deposits from the et al. 2012a). The southern West Junggar developed southern West Junggar in a bid to (1) compare their min- several northeast-trending faults including the Barluk, eralization types, ore-forming ages, ore-bearing magma Mayile, and Darbut faults. The documented Suyunhe genesis, and tectonic setting and (2) determine the relation- W-Mo deposit occurred in the Barluk Mountains, located ship between the North Balkhash and the southern West in the west of the Mayile fault and the documented Junggar ore belts and implications for mineralization in Baogutu Cu and Hongyuan Mo deposits occurred in the CAOB. International Geology Review 1663

Kelamay Region, located in the east of the Mayile fault et al. 2012; Figure 1). The strata are divided into three (Figure 2). units, the ﬁrst being the Precambrian metamorphic base- The Barluk Mountains are located in the western ment composed of schist, gneiss, amphibolite, and quartz- part of the southern West Junggar (Figure 2). Fossil- feldspathic schist, exposed in the north and west of Central dated Devonian strata occur widely in the Barluk Kazakhstan. This unit is the most prominent unit of the Mountains close to the China–Kazakhstan border Kokchetav Massif in north-central Kazakhstan. The second (Figure 2; BGMRXUAR 1993), and are the volcano- unit is Palaeozoic folded sedimentary and metamorphic sedimentary strata of the Middle Devonian Barluk and rocks, which change from assemblages of volcanogenic Tieliekede Groups. The Barluk Group is composed of silicic, terrigenous clastic, and carbonate rocks in the siltstone, tuff, and minor basalt; the Tieliekede Group Cambrian and Ordovician, to terrigenous clastic or shallow consists of greywacke, tuffaceous mudstone, and tuffa- marine clastic rocks in the Silurian and Devonian, to vol- ceous siltstone. These Devonian sequences are intruded canic rocks of dacite and rhyolite intercalated with tuff in by Carboniferous–Permian intrusions in the Barluk the Carboniferous, and to the basalt-rhyolite and terrestrial Mountains. Carboniferous intrusions include peridotite, volcanic tuff in the Permian. The third unit is widespread gabbro, diorite, and quartz diorite stocks, while Permian cover of Mesozoic and Cenozoic sandstone and mudstone. intrusions include diorite, quartz diorite, and adamellite Central and East Kazakhstan display a large oroclinal bend stocks (BGMRXUAR 1993). Structurally, the Barluk of Palaeozoic foldbelts, which range from Cambrian to Mountains are characterized by the northeast-trending Ordovician ages in the outer part to Carboniferous in the Barluk fault, although NE- and NW-trending structures are central part (Popov 1996; He and Zhu 2006;Zhuet al. also present. 2007; Figure 1B). The Kelamay Region, located in the eastern part of Intrusive rocks emplaced from the Proterozoic to the southern West Junggar, is characterized by the occur- Permian, consisting primarily of late Palaeozoic granitoid rence of lower Carboniferous volcano-sedimentary strata rocks. Serykh (1996) subdivided the granitoid series in (Figure 2). There are three early Carboniferous strati- foldbelts of Central and East Kazakhstan into early or syn- graphic units, from oldest to youngest: the Tailegula, orogenic and late or post-orogenic series. Four series of Baogutu, and Xibeikulasi Groups (Shen and Jin 1993). volcanic and intrusive rocks were recognized by Popov The Tailegula Group consists of a succession of basic (1996): pre-, early, main, and late orogenic. Most of the volcanic and volcaniclastic rocks intercalated with chert. Cu-Mo and Au deposits in the belt are associated with The Baogutu Group includes tuffaceous siltstone, silt pre-orogenic and early orogenic diorite, granodiorite, and tuff, and felsic tuff, while the Xibeikulasi Group consists adamellite intrusive rocks. In contrast, stockwork and vein of greywacke. These early Carboniferous sequences are Mo deposits and scheelite-bearing W deposits are related intruded by ore-bearing diorite stocks at about ∼320 Ma to main orogenic granite and leucogranite, and polymetal- (Tang et al. 2009; Shen et al. 2012b) and voluminous bar- lic Mo-W-Be-Bi mineralization is accompanied by late ren post-collisional granite batholiths at about ∼310 Ma orogenic leucogranitic plutons (Popov 1996; Heinhorst (Chen and Jahn 2004;Hanet al. 2006). The Baogutu and et al. 2000). Hongyuan intrusions occur in the south of the Darbut fault. There are a number of irregularly distributed remnants The southern West Junggar is characterized by of lower Palaeozoic oceanic crust in Central Kazakhstan. the occurrence of several ophiolite belts (Figure 2). However, in contrast to examples from collisional oro- A Cambrian island arc ophiolite crops out at Tangbale gens, these ophiolite rocks do not mark interplate suture (Jian et al. 2005), together with Ordovician and Silurian zones (Sengör et al. 1993) and show geochemical features sedimentary rocks. Newly discovered Kalamay ophiolite of fore-, back-, or intra-arc oceanic crust (Kröner et al.

Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 mélanges were formed during the Ordovician (He et al. 2007). Ophiolite belts in Central Kazakhstan comprise only 2007). A Silurian ophiolite is found at Maila (Wang et al. the topmost layers of palaeo-oceanic crust, especially the 2003), while the Darbut ophiolite belt is Devonian in age deep-sea sediments and volcanic rocks. (Xu et al. 2006). The youngest reported ophiolite at Maliya has a Carboniferous age (Dong and Wang 1990). Most 3. Deposit geology ophiolites show contact relationships with the Devonian to lower Carboniferous volcanic–sedimentary strata via 3.1. Porphyry Cu deposits faults. 3.1.1. Baogutu Cu deposit The Baogutu copper deposit is located about 60 km south- west of Kelamayi City (Figure 2). It contains 630 kt Cu 2.2. North Balkhash metal at an average grade of 0.28%, 18 kt Mo metal at North Balkhash, located in Central and East Kazakhstan, an average grade of 0.011%, and 14 t Au metal at an exposes integrated Palaeozoic strata, plutons, and volcanic average grade of 0.1 ppm. Our previous work recognized rocks (Heinhorst et al. 2000; Chen et al. 2010a;Cao two mineralized intrusive phases at Baogutu, which are 1664 P.Shen et al.

the main-stage granular to porphyritic diorites and minor quartz-sericite rocks (Figure 4D), propylitic, and the latest late-stage diorite porphyries (Shen et al. 2010a, 2010b; quartz-kaolinite argillic alteration that is closely related to Figure 3). They intrude the lower Carboniferous Baogutu the intrusion of ore-bearing porphyritic granodiorite; the and Xibeikulasi groups. third is restricted in its occurrence by the late dikes and The main-stage diorites host the bulk of the Cu-Au- includes potassic alteration and mica-quartz-tourmaline Mo mineralization at Baogutu. They have been overprinted alteration. The second alteration is associated with Cu- by three alteration assemblages, including an early potassic Mo mineralization (Figures 4D and 4E). Dominant vein (biotite) assemblage that occurs in the centre of the deposit. stockworks and hydrothermal breccias occur in Kounrad. A propylitic assemblage surrounds the potassic zone con- The main mineral assemblages of the deposit are pyrite, centrically. Both of these alteration assemblages have chalcopyrite, chalcocite, and molybdenite. been overprinted locally by phyllic alteration (Shen et al. 2010a, 2010b). Potassic alteration associated with most 3.1.3. Borly Cu deposit Cu-Au mineralization is predominant in the diorites and The Borly porphyry Cu deposit is situated 60 km to the in the wall rocks. Intense phyllic alteration is predomi- north of Balkhash City and 45 km from the Kounrad nant in the diorites and is associated with most Cu-Mo Cu deposit. It lies mainly in the southern part of the mineralization. The dominant disseminated mineraliza- Tokrausky synclinorium, and its Cu reserves amount to tion (Figure 4A) and lesser amounts of vein stockworks some 600 kt Cu @ 0.34%, associated with Mo (average (Figure 4B) occurred in Baogutu. The main mineral assem- grade 0.11%), Au (average grade 0.03 ppm), Ag (average blages of the deposit are pyrite, chalcopyrite, pyrrhotite, grade 1341 ppm), Re (average grade 0.42 ppm), and Se and molybdenite (Figure 4C). (average grade 3.01 ppm), with a total Cu:Mo ratio of 50:1 (Popov 1996). 3.1.2. Kounrad Cu deposit The strata in the Borly area include the lower Carboniferous Karkaralinskaya and upper–middle The Kounrad porphyry Cu deposit is situated 10 km to the Carboniferous Keregetass groups. The former is a north of Balkhash City. It lies in the southern part of the suite of lithic-crystal tuff, lava, and subvolcanic rocks, Tokrausky synclinorium in Central Kazakhstan. Kounrad while the latter includes a suite of dacite, sometimes is spatially related to a large massif of silicified volcanic trachdacite or andesite-dacite ignimbrite, microlitic tuff, rocks, and it contains more than 8 Mt Cu metal at an aver- tufflava, lava, and subvolcanic rocks. age grade of 0.61%, associated with Mo (average grade The centre of the Borly deposit is the Borlinksy 0.0035%), Au (average grade 0.017 ppm) (Zhukov et al. apophysis of the Kyzylzhalsky intrusion. The Borlinksy 1997), and a total Cu:Mo ratio of 115:1 (Popov 1996). apophysis contains three phases: (1) quartz diorite, (2) the Early Carboniferous sedimentary-volcanic units main phase, biotite amphibole granodiorite (Figure 4G), occurred in the Kounrad area and formed a volcanic appa- and (3) light-coloured granite-porphyry. They are cut by ratus. The strata include Late Devonian and Carboniferous a granodiorite stock. The intrusion of that rock body sedimentary, volcanogenic-sedimentary, and volcanic was accompanied by intensive cryptoexplosive breccia- units. They are intruded by the Toktay intrusive complexes tion, hydrothermal alteration, and the formation of quartz- of Carboniferous age (Figure 5). The Toktay intrusive sulphide stockworks. The youngest magmatic assemblage complexes are subdivided into three phases: (1) gabbrodi- is the alkaline granite porphyry dikes and subvolcanic orite porphyry, which is a small stock; (2) the main phase, rocks in the early Permian Zhaksitagalinsky complex biotite-amphibole granodiorite, porphyritic granodiorite, (Abdulin et al. 1998). and granodiorite porphyry; and (3) fine-grained granite The Borlinksy apophysis hosts the bulk of the Cu- Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 and granite porphyry dikes. The second stock is the main Mo mineralization (Figures 4H and 4I) at Borly. It has ore-bearing one, which defines an area of mineralized been overprinted by three alteration assemblages: an early × rocks approximately 1100 m 800 m. basic alteration (K-feldspar, chlorite, quartz, epidote), a The Kounrad area is characterized by an irregular middle acidic alteration (quartz, sericite, chlorite, and cal- elliptical caldera ring-fracture, which is influenced by sev- cite), and a late basic alteration (quartz and calcite). Early eral NE–NW-trending faults. The ore-bearing stocks and basic and middle acidic alteration are associated with associated copper orebodies are controlled by the caldera most Cu mineralization. The main mineral assemblages ring-fracture. of the deposit are pyrite, chalcopyrite, and molybdenite Almost all rocks forming the deposit have, to a vari- (Figures 4H and 4I). able extent, been affected by hydrothermal alteration. They can be subdivided into three groups (Kudryavtsev 1996): the first is represented by the quartz-sericite and 3.1.4. Aktogai Cu deposit quartz-sericite-diaspore altered rocks that resulted from The Aktogai porphyry Cu deposit is situated 22 km east post-volcanic hydrothermal activity; the second comprises of Aktogai railway station (Figure 6) and contains 12.5 Mt International Geology Review 1665 Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013

Figure 3. (A) Geological map of the Baogutu porphyry Cu deposit showing the intrusion complex. Line WE01 shows the location of the section shown in (B), dots indicate the position of drill holes. (B) Geologic cross-section along WE01 showing the host rocks to the Baogutu deposit and the copper ore bodies (Shen et al. 2010a). 1666 P.Shen et al.

Figure 4. Photographs of ore-bearing rocks and mineralization. Baogutu Cu deposit: (A) disseminated ore in medium-grained diorite with disseminated chalcopyrite and biotite; (B) vein ore, Q-Cpy veinlets overprinted in the disseminated mineralization in diorite; (C) vein ore, Q-Cpy-Mo veins. Kounrad Cu deposit: (D) vein ore, Q-Cpy veinlets overprinted in the disseminated mineralization in granodiorite; (E) disseminated ore with disseminated Mo. Aktogai Cu deposit: (F) disseminated mineralization in granodiorite. Borly Cu deposit: (G) granodiorite; (H) vein ore, Q-Cpy veins; and (I) vein ore, Q-Mo veins. All photographs under natural light. Note: Q, quartz; Cp, chalcopyrite; Mo, molybdenite. Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013

Figure 5. Geological map of the Kounrad porphyry Cu deposit showing the intrusion complex and associated wall rocks (from Zhukov et al. 1997). International Geology Review 1667

Figure 6. Generalized geological map of the North Balkhash region (modiﬁed after Chen et al. 2010a).

Cu metal with an average of 0.3% Cu (Cooke et al. 2005), The strata in the Aktogai include the upper 271 kt Mo metal at an average grade of 0.01%, and 60 t Carboniferous–lower Permian Koldarskaya Group Au metal at a grade of 0.007–0.40 ppm, associated with and middle–upper Carboniferous Keregetasskaya Group Ag (average grade 1.8 ppm), Re (average grade 0.24 ppm), (Figure 7). The Koldarskaya Group includes a suite of and Se (average grade 1.8 ppm) (Chen et al. 2010b). sedimentary rock, volcano-sedimentary rock, and minor Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013

Figure 7. Geological map of the Aktogai porphyry Cu deposit area showing the Aktogai, Aidarly, and Kyzylkiya Cu deposits (from Zhukov et al. 1997). 1668 P.Shen et al.

acidic tuffs. The Keregetasskaya Group is a suite of Phenocrysts are plagioclase and quartz and minor biotite andesite and minor rhyolite and stone and siltstone. Cu-Mo and hornblende; the groundmass exhibits a subhedral tex- mineralization is related to granodiorite porphyry and ture with plagioclase, quartz, and minor biotite. Granite quartz diorite porphyry (Figure 4F) and other small, has a hypidiomorphic-granular texture and consists of pla- shallow, intrusive bodies in the early Carboniferous gioclase, microcline, and quartz (Figure 9A). Associated granodiorite batholith, covered by Carboniferous–lower hydrothermal alteration consists of quartz vein and greisen Permian volcano-sedimentary rocks (Figure 7). (quartz-muscovite, Figure 9B) occurring in the granite. The Associated hydrothermal alteration consists of silici- granite is associated with W-Mo mineralization. ﬁcation in the core, K-silicate alteration, quartz-sericite The orebodies are mainly hosted in the wall rocks alteration within the stock, and propylitization in the wall- (Figure 8), which include tuff and tuffaceous siltstone. rock. The veinlet disseminated orebody mainly developed The orebodies have vein and lenticular forms and have in the quartz-sericite alteration. The opaque minerals found no distinct boundaries with country rocks, showing gra- under the microscope are mainly pyrite, chalcopyrite, dational contact relationships. The orebodies occupy an molybdenite, and minor pyrrhotite and chalcocite. area of 3200 m × 600 m. Five tungsten orebodies, 12 molybdenum orebodies, and one tungsten-molybdenum 3.2. Quartz-vein greisen W-Mo deposits orebody have been recognized in the Suyunhe ore dis- 3.2.1. Suyunhe W-Mo deposit trict. The ore types are W ore, Mo ore, and W-Mo ore (Figures 9C and 9D). The dominant types of ore mineral The Suyunhe W-Mo deposit lies about 80 km southeast of assemblage are quartz-molybdenite, quartz-scheelite, and Yumin town (Figure 2). It is a newly discovered W-Mo quartz-molybdenite-scheelite. Ore minerals mainly include deposit and is under exploration by the local geological scheelite, molybdenite, and minor chalcopyrite and pyrite. team. Gangue minerals are mainly quartz, muscovite, sericite, Fossil-dated Devonian strata occur widely in the and calcite. The W-Mo mineralizations occur mainly in Suyunhe area. They are the volcano-sedimentary strata of quartz veins and quartz veinlets. the Middle Devonian Barluk Group, composed of siltstone, tuff, and minor basalt. The Barluk Group is intruded by Carboniferous–Permian intrusions, which occupy localized 3.2.2. Hongyuan Mo deposit dilatant sites provided by the intersection of NNE- and The Hongyuan Mo deposit lies about 15 km north of NEE-trending faults (Figure 8). They include plagiogranite Kelamay City. It is a newly discovered Mo deposit and is porphyry and granite, based on our microscope observa- under exploration by the local geological team (Figure 2). tion. The plagiogranite porphyry has a porphyritic texture. The Early Carboniferous Tailegula Group occurs in the Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013

Figure 8. Schematic geological map of the Suyunhe quartz-vein W-Mo deposit (modiﬁed from local geological team, 2009). International Geology Review 1669

Figure 9. Photographs and microphotographs of ore-bearing rocks and ores from the quartz vein-greisen W-Mo deposits in the southern West Junggar and the North Balkhash ore belts. Suyunhe W-Mo deposit: (A) alkali granite; (B) greisenization alkali granite; (C) Q-Mo veins; (L) Q-Sch veins. Hongyuan Mo deposit: (E) porphyritic granite; (F) greisenization porphyritic granite; (G) Q-Ms vein; (H) Q-Mo vein. East Kounrad W-Mo deposit: (I) alkali granite. Akshatau W-Mo deposit: (J) Q-Mo-Be veins. Zhanet Mo deposit: (K) alkali granite: (L) Q-Mo veins. All photographs taken under natural light except A, B, E, and F, which were taken under transmitted lights. Note: Pl, plagioclase; Or, K-feldspar; Q, quartz; Mo, molybdenite; Sch, scheelite; Be, beryl.

Hongyuan area and is composed of tuff and tuffa- granite (Figure 9G). Greisenization (quartz and muscovite) ceous siltstone intercalated with basic volcanic rocks. The occurs in the granite stock (Figure 9F), while molybdenite Tailegula Group is intruded by Permian intrusions, includ- mainly occurs in quartz veins and ﬁssures. The ores contain Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 ing Kelamay granite pluton and Hongyuan granite stock. molybdenite, pyrite, quartz, muscovite, sericite, and very The Hongyuan granite stock is associated with Mo miner- minor chalcopyrite (Figure 9H). alization. Previous work has suggested that the Hongyuan Mo 3.2.3. East Kounrad W-Mo deposit deposit is a porphyry Mo deposit (Li et al. 2012). Based on our present study, we consider it to be a quartz vein- The East Kounrad W-Mo deposit lies about 11 km east of greisen Mo deposit. The Hongyuan granite stock consists the Kounrad porphyry Cu deposit. It is an underground- of granite and porphyritic granite based on our microscope mined W-Mo deposit, but the mine is now abandoned. The observations (Figure 9E). Granite has a hypidiomorphic- East Kounrad W-Mo deposit has reserves of 200–250 kt, granular texture and consists of plagioclase, microcline, averaging 0.056% Mo. and quartz. Porphyritic granite is the same as granite in The East Kounrad W-Mo deposit is associated with the composition but has a porphyritic-like texture. The ore- syenogranite stock (Figure 9I). The ore deposit occurs in body occurs in the Hongyuan granite stock. In addition, endo- and exocontact zones of syenogranite. It is of the many quartz-muscovite veins occur in the ﬁssures of the quartz vein-greisen type, with the major ore minerals being 1670 P.Shen et al.

wolframite and molybdenite. W-Mo mineralizations occur occurring inside granite cupolas or at their wings and mainly in quartz veins and quartz veinlets, and also at the ridges of different sizes. Enriched deposits are most easily tops of cupolas and in greisens surrounding quartz veins found at the tops of granites in mono-dome structures (Burmistrov et al. 1990). The main mineral assemblages of (Daukeev et al. 2004). The ore-forming process has mainly the deposit are scheelite, wolframite, molybdenite, apatite, undergone two stages and four phases: the first stage is phenakite, beryl, biotite, muscovite, bismite, bismuthinite, the pneumatolytic hydrothermal stage, comprising the calcite, chalcopyrite, ferromolybdite, fluorite, prosopite, molybdenite quartz phase (440–340◦C) and a complex helvite, microcline, pyrite, phlogopite, powellite, quartz, rare-metal phase (480–250◦C); the second stage is the rhodochrosite, salite, and topaz. real hydrothermal stage, containing the galena-sphalerite- quartz phase (310–150◦C) and the calcite-fluorite-quartz phase (180–60◦C) (Yefimov et al. 1990). The ores contain 3.2.4. Akshatau Be-W-Mo deposit molybdenite, wolframite, fluorite, and beryl (Figure 9J). The Akshatau large-sized W-Mo deposit occurs in the southeastern part of the Zhaman–Sarysu Anticlinorium near its boundary with Toqrau Basin, 150 km from 3.2.5. Zhanet Mo deposit Balkhash City (Figure 6). It is a disseminated quartz vein- The Zhanet Mo deposit is a medium-sized quartz vein- greisen Be-W-Mo deposit and is closely related to the tops greisen Mo deposit located 120 km to the northwest of of the Carboniferous granite complex in both endocontacts Balkhash City (Figure 6). It was first explored in 1948 and and exocontacts, having resources as follows: 65.5 kt of was mined for some time, but at present mining is tem- 0.10–0.30% WO3, 17.5 kt of 0.04–0.07% Mo, and 16.0 kt porarily suspended. of 0.03–0.07% Be (Yefimov et al. 1990). The orebody occurs at the intersection of the Akzhal– The Akshatau deposit occurs within Permian Aksoran and Akbastay faults. The network Mo-W min- leucogranites of the Akshatau multi-stage complex eralization is associated with syenogranite porphyries. that intrude Carboniferous volcanic rocks (Figure 10). Molybdenite mainly occurs in syenogranite porphyries The Akshatau multi-stage complex is controlled by linear (Figures 9K and 9L) and in late-stage quartz veins and and circular faulted structures and by the intersection fissures. In the late-stage quartz veins, molybdenite is by structural belts of different trends (Burmistrov et al. associated with fluorite. 1990). The Akshatau deposits are closely related to the The ores contain molybdenite, wolframite, topaz, flu- tops of ore-forming intrusives in both endo- and exocon- orite, and beryl. The main ore mineral is molybdenite tacts. The greisen bodies consist of root, intermediate, (Figure 9L), which also has high contents of rare-earth and and front zones. Most lie within the intermediate zone, rare elements. Molybdenites occur mainly in Mo-bearing Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013

Lower Carboniferous Permian Akshatau intrusion complex Hydrothermal volcanic rocks Stage 1 coarse – grained Stage 2 medium – quartz rock porphyritic granite grained granite Carboniferous Hornfelsed subvolcanic rocks Stage 1 fine – grained Stage 2 fine – grained zone porphyritic granite leucogranite Carboniferous quartz Greisenization monzonite and granodiorite zone

Figure 10. Schematic geological map of the Akshatau quartz-vein greisen W-Mo deposit (modiﬁed from Daukeev et al. 2004). International Geology Review 1671

granite-porphyries and in late-stage quartz veins and ﬁs- Sciences (CAS) in Beijing. The analytic procedures are sures assuming disseminated and veined shapes. In the similar to those described by Shen et al. (2012a). Major late-stage quartz veins, the molybdenites are associ- elements were analysed by XRF-1500 Sequential X-ray ated with ﬂuorite. Wall-rock alterations include potassic- Fluorescence Spectrometry, with wet chemical determina- alteration (e.g. K-feldspathization, biotitization), pyritiza- tion of FeO and loss-on-ignition. A PQ2 Turbo inductively tion, greisenization, and epidotization. Pegmatite veins coupled plasma mass spectrometer (ICP-MS) was used to formed in the late stage. analyse trace elements and REE.

4. Methods and results 4.1.3. Nd isotopes 4.1. Methods The four samples from the Suyunhe and Baogutu deposits 4.1.1. Molybdenite Re-Os dating were selected for Sm and Nd isotope composition analyses. Measurements were carried out at the Institute of Previous works have obtained the Re-Os ages of Geology and Geophysics, CAS. Sm and Nd isotope com- molybdenites from the Borly Cu deposit, the East Kounrad, positions were analysed according to a procedure simi- Zhanet, and Akshatau W-Mo deposits in the North lar to that described by Chen et al. (2002). Procedural Balkhash (Chen et al. 2010), and the Baogutu Cu (Shen blanks were <100 pg for Sm and Nd. The 143Nd/144Nd et al. 2012b) and Hongyuan Mo deposits (Li et al. 2012) in ratios to 146Nd/144Nd = 0.7219. Typical within-run pre- southern West Junggar. For comparison, in this study, cision (2 σm) for Nd was estimated at ±0.000013. we measured the Re-Os ages of molybdenites from the The values measured for the JMC Nd standard were Suyunhe W-Mo deposit in southern West Junggar. 143Nd/144Nd = 0.511937 ± 7(2σm, n = 12) during the The five molybdenite samples used for Re-Os isotope period of data acquisition. dating were collected from the Suyunhe W-Mo deposit. Re-Os isotope dating of the molybdenite samples was performed at the Re-Os Isotope Chronology Laboratory, 4.2. Results National Research Centre for Geoanalysis. The chemical 4.2.1. Molybdenite Re-Os ages separation and processing processes of Re and Os, as well as the mass spectrometry technology, have been described The concentrations of Re and Os and the osmium isotopic by Du et al. (2004). The isotope ratio was determined using compositions of five samples of the Suyunhe sulphide 187 187 the TJA X-series ICP-MS at the National Research Centre ores are presented in Table 1. Total Re and Os for Geoanalysis. The uncertainties of model ages also concentrations vary from 49 to 113 ppm and from included the uncertainty of the decay constant (1.02%), 245 to 581 ppb, respectively. The Re-Os model ages and the confidence level was also 95%. Ludwig’s (2003) of the five molybdenites obtained in the experiment are ± ± ± method was used to process the Re and Os isotope data 302.6 4.9 Ma, 304 4.5 Ma, 306.2 5.1 Ma, ± ± relating to molybdenites and to obtain the average ages of 296.1 4.4 Ma, and 296.5 4.4 Ma, with a mean value ± Re-Os. of 300.7 4.1 Ma, which is interpreted as the age of molybdenite crystallization during the formation of the Suyunhe W-Mo deposit. 4.1.2. Major and trace elements Samples used in this paper were petrographically collected from drill cores for chemical analyses at Suyunhe and 4.2.2. Major and trace elements Baogutu. They are the four granites at Suyunhe and three Major and trace element concentrations of the studied sam-

Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 diorites at Baogutu. Measurements were carried out at the ples are listed in Table 2 and plotted in Figures 11–13. For Institute of Geology and Geophysics, Chinese Academy of comparison, data from the Kounrad, Borly, and Aktogai Cu

Table 1. Re-Os isotope composition of molybdenites from the Suyunhe W-Mo deposit in the southern West Junggar ore belt.

Re (μg/g) Normal Os (ng/g) 187Re (μg/g) 187Os (ng/g) Model age (Ma)

Sample no. Weight (g) Measured 2σ Measured 2σ Measured 2σ Measured 2σ Measured 2σ

SyMo-2 0.00635 89.53 0.95 0.031 0.0347 56.27 0.6 284.4 2.5 302.6 4.9 SyMo-2 0.01004 95.77 0.92 0.0475 0.213 60.2 0.58 305.6 2.4 304 4.5 SyMo-4 0.00558 180.9 2 0.036 0.121 113.7 1.2 581.6 5.5 306.2 5.1 ZK03-180 0.00836 78.91 0.73 0.024 0.1344 49.6 0.46 245.2 2.1 296.1 4.4 ZK03-159 0.00573 105.3 0.9 0.0835 0.2808 66.19 0.54 327.8 3 296.5 4.4

Note: Uncertainty for the calculated ages is 1.02% at the 95% conﬁdence level. 1672 P.Shen et al. ) b 7.28 1.35 90.2 -9(3) Grano diorite P Xh080912 ( Continued Borly b 0.41 0.45 3.81 3.55 0.19 0.19 5.2 7.37 7.43 2.17 2.23 5.93 4.58 0.892.790.41 0.83 2.78 1.3 0.42 1.340.211.56 1.41 0.21 1.97 4.54 3.62 26.2 19 13.2 14.6 43.214.4 19.3 17.9 59.821.8 40.8 17.7 -9(2) Grano 188 139 522 515 270 414 218 diorite P Xh080912 lts. d 3 Quartz diorite P d 4 Grano diorite P d 2 Grano diorite P d 5 Grano diorite P d 1.69 1.68 2.24 1.83 2.37 1.76 2.16 0.36 0.45 0.43 0.41 0.38 0.51 0.36 1 Kounrad Qrano diorite c Qrano diorite KoG25 b 4.99 4.56 0.53 0.54 0.44 0.5 0.48 0.44 0.71 0.67 0.48 7(1) Quartz diorite P Xh080910- b P 2(1) Adamellite Xh080910- a 144 ZK211- a 60 ZK211- a 4 BGT5- a 3 BGT5- a 2 Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 diorite Diorite Diorite Diorite Diorite Quartz BGT5- Baogutu a 1 BGT5- 295 ZK202- 616 ZK201- 4.93 4.160.07 4.69 0.12 4.35 0.08 3.91 0.04 4.41 0.06 4.81 0.03 5.01 0.03 4.51 0.09 1.82 0.08 2.53 0.08 2.19 0.11 1.24 0.08 1.79 0.17 2.19 0.04 1.65 0.06 1.92 0.3 2.36 0.14 1.6 0.06 0.15 5.25.1 5.3 7.21 4.2 7.45 1.87 7.56 3.44 5.441.75 1.64 7.52 1.57 1.24 7.85 1.65 4.76 7.07 1.51 4.55 6.94 1.59 1.31 1.51 1.23 1.49 2.05 3.45 1.56 1.57 4.38 3.05 2.34 2.63 1.96 0.92 2.15 1.90 3.09 1.93 1.90 0.61 3.03 2.46 2.19 2.11 1.86 1.95 2.39 1.33 1.45 1.132.747.69 1.22 3.09 1.78 1.1 3.273.04 4.58 0.95 2.483.12 3.9 2.280.89 1.51 3.23.03 3.69 0.99 4.10.61 1.29 0.89 2.693.63 3.13 3.9 0.920.72 4.15 0.59 1.232.07 5.01 2.69 3.14 3.28 0.65 3.790.34 0.6 3.2 0.59 1.211.94 1.68 2.76 3.46 3.36 2.11 2.770.33 0.25 0.53 0.92 2.69 0.66 4.030.17 1.48 1.84 2.96 2.91 2.87 2.91 4.313.87 0.27 0.3 0.39 1.27 0.57 2.661.89 0.18 1.79 0.89 1.71 2.5 3.78 3.45 4.81 5.09 0.31 0.55 1.14 0.22 0.49 3.18 2.17 0.22 1.45 1.57 1.37 3.53 3.091.73 3.15 4.87 0.23 0.55 0.98 0.21 0.59 4.45 1.72 0.14 1.36 2.31 6.51 1.74 2.71 3.16 1.13 4 2.96 0.21 0.41 1.18 0.24 0.62 3.29 0.21 1.04 1.56 1.72 4.4 3.39 2.42 1.24 8 2.97 0.23 0.49 0.27 0.49 4.09 0.15 1.59 0.85 0.91 1.35 3.38 2.84 2.61 2.98 0.23 2.57 0.2 0.56 1.94 0.14 0.38 1.29 1.2 1.53 3.9 2.77 0.19 1.99 0.89 3.4 0.22 1.58 0.16 1.43 0.39 2.83 1.16 4.14 0.21 2.51 6.27 0.45 1.22 0.21 0.91 0.16 2.42 3.51 1.17 3.86 2.52 2.71 0.51 0.17 2.61 0.38 1.54 4.34 0.91 1.7 2.01 10.4 0.22 1.57 0.41 5.14 1.16 0.25 2.84 1.37 0.16 16.6 1.14 13.6 0.15 3.52 0.8 12.7 7.7 3.86 2.57 3.422.16 4.07 1.03 5.04 0.75 4.41 0.72 4.16 0.65 4.46 0.67 4.75 0.37 3.87 1.4 4.03 1.31 4.71 2.42 3.39 3.15 4.11 2.25 4.3 2.03 3.84 2.111.39 5.39 2.66 0.61 4.63 2.45 0.77 4.63 2.67 1.13 2.24 1.03 3.01 0.55 3.28 2.66 0.4 0.56 1.29 1.75 3.59 1.7 2.56 2.61 1.16 1.740.860.13 2.03 0.94 0.21 0.870.42 0.98 0.21 0.62 0.38 0.82 0.18 1.92 0.46 0.69 0.14 1.5 0.64 0.88 0.21 0.47 0.83 2.93 0.1 0.67 0.88 0.2 3.14 0.75 0.88 0.24 0.45 4.29 0.5 0.43 1.93 0.19 2.15 0.52 0.14 2.34 0.49 0.19 2 0.23 2.39 0.18 3.11 0.21 0.18 2.87 0.27 0.19 0.15 263 99.83 99.92 99.89 99.65 99.52 99.53 99.54 99.34 99.71 102 101.7 99.5 100.8 100.1 98.78 100.1 100.2 103.6 102.0 10.422.4 13.813.7 29.3 11.8 16.9 29.6 10.7 17.7 29.7 10.8 18.6 22.9 8.8 14.9 28.1 5.6 19.2 16.8 10.0 13.8 21.2 14.1 13.1 29.550 18.2 15.9 36 31.7 17.6 36 21.7 48.1 94 17.7 18.5 38.8 132 17.8 85 93 58 93 140 156 85 20.6 16.4 17.6 15.1 14.5 15.4 17.4 13.3 14.9 12.1 16.1 11.1 57.7215.29 57.13 15.81 57.84 16.04 58.95 17.88 62.05 15.73 59.98 17.76 59.92 18.07 55.68 16.92 57.72 17.01 65.24 16.56 63.86 16.68 64.48 16.14 67.3 16.9 66.39 16.53 66.18 15.07 66.8 16.8 63.51 17.32 66.51 16.81 65.94 15.98 129 34.4 35.2429 43.3 486 14.6 262 36.4 222 13.2 354 40.0 240 41.2 221 29.4 411 418 93.7 532 69 877 528 542 655 632 746 559 707 748 722 739 487 786 606 ZK211- 3 3 5 O 2 2 O O # O 2 O 2 2 2 2 Table 2. Major (wt.%) and traceDeposit element (ppm) abundance of rocks from the ore-bearing intrusions inSample the southern West Junggar and North Balkhash ore be RockSiO DioriteAl DioriteFe DioriteFeO Diorite MgO CaO Na K MnO TiO P Loi Total Mg A.R. Rb Sr Y Nb Cs Ba La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Ta Pb Th U Zr Hf International Geology Review 1673 c 9.2 7.5 0.06 0.28 36.6 23 19.5 Leuco granite AQSG3 c Akshatau Leuco granite AqsK9 b 14- Alkali 10(1) granite Xh0809 b 15- 5(5) Alkali granite Xh0809 b 0.56 0.32 0.23 0.40 0.11 0.35 5.03 5.64 4.1 5.97 6.7 15- 25.6 36.9 21.3 26 5(3) llite P 463 25.7 19.8 34 618 626 649 397 543 197 120 106 148 137 Zhanet Adame Xh0809 c P 10 Syeno ZH-2- granite c KoeK16 b 0.25 0.27 4.38 2.54 10- 14 15 Alkali 10(1) 271 24 144 184 146 68 granite Aplite Xh0809 East Kounrad e 1.96 1.74 5.9 19.1 5.42 4.85 34.3 9 Syeno (2012). granite P et al. Cao e Alkali granite ); 1996 221 SY4-1 EK-1 Alkali ZK03- granite Suyunhe Kudryavtsev ( 215 d Alkali ZK03- granite (2000); 0.5 0.45 0.65 0.1 1.95 2.08 1.97 1.41 2.37 1.3 2.73 9.17 3.27 1.8 2.3 0.26 0.32 0.28 0.55 3 3.47 3.88 3.19 214 Alkali ZK03- granite et al. c 6 8.35 8.13 9.86 8.29 phyre Grano AQ13 Heinhorst c c ); Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 nd nd stock AQ7 Porphyry 2012 .( b 19- 5(5) llite P et al Adame Xh0809 Liu b Aktogai b ); 0.75 0.92 2.8 3.21 0.38 0.46 2.65 2.66 1.45 1.43 6.13 5.66 5.62 5.48 0.60 0.57 19- 63.2 90.9 33 41 153 166 160 142 98.5 98.5 48 44 133 125 128 112 5(4) Grano 796 1049 994 934 155 182 303 141 Xh0809 diorite P 2009 ( e et al. Grano A2-6 diorite P e Shen a 1.51.42 1.58 2.910.02 1.45 1.91 0.02 1.61 1.63 0.02 0.66 3.122.87 0.02 0.9 2.8 2.19 0.05 0.23 0.85 2.53 0.08 0.28 1.19 0.03 2.98 0.33 0.92 2.31 0.03 0.16 2.49 0.04 0.63 4.71 0.02 0.2 0.63 4.72 4.52 0.12 0.05 0.78 0.07 0.57 5.15 0.06 0.51 1.09 0.03 4.59 0.49 2.18 0.05 0.05 0.48 4.38 0.04 0.16 0.54 4.94 0.02 4.43 0.1 0.06 0.55 3.56 0.04 0.8 4.54 5.98 0.03 5.09 4.39 1.82 1.88 5.74 4.3 1.05 0.86 0.872.91 12.4 3.621.75 0.56 2.92 2.510.34 1.55 3.08 2.140.14 1.17 0.290.94 1.46 1.92 2.16 0.11 0.27 0.71 0.26 1.45 2.05 1.2 0.11 0.3 0.8 0.87 2.68 0.62 1.24 0.11 0.18 1.05 2.77 0.78 2.35 0.38 0.08 0.23 3.2 0.55 2.52 0.94 2.46 0.1 0.679 0.69 3.37 1.84 2.4 1.63 0.77 0.48 3.47 3.3 0.86 0.74 0.50 1.57 1.86 3.94 0.4 0.49 2.24 0.53 3.62 1.98 1.7 0.51 0.38 1.43 0.51 3.01 0.33 1.32 2.76 0.7 0.17 1.08 0.23 1.21 0.35 4.23 0.4 0.09 0.12 2.29 1.02 1.01 0.52 2.29 0.08 3.2 0.74 1.23 0.94 3.85 0.31 0.78 2.44 1.86 0.27 0.99 0.73 0.93 6.45 0.22 0.94 0.27 0.91 2.56 1.24 0.16 0.3 1.32 1.55 0.74 0.22 2.33 1.01 0.24 2.44 4.213.96 4.38 2.86 3.83 3.65 4.5 4.29 4.82 3.13 4.789.77 3.65 3.44 8.25 4.45 3.49 8.82 4.894.45 4.04 9.11 4.47 5.47 4.80.78 3.75 4.25 4.52 6.20.33 0.87 3.83 4.33 23.8 0.31 4.73 0.830.93 2.58 25.8 0.28 3.85 0.89 4.58 0.75 2.940.15 24.9 3.84 0.59 0.29 4.79 0.82 3.328.06 0.11 0.18 2.91 0.577.25 17.2 5.99 0.83 3.321.59 8.68 0.12 0.218 0.21 4.3 4.99 4.88 0.51 3.53 3.45 8.19 0.22 0.49 0.12 10.9 3.31 4.99 4.42 0.64 10.2 0.78 0.08 0.32 1.98 0.54 3.6 5.52 2.45 5.42 7.86 8.7 0.84 0.09 0.52 0.18 2.1 2.75 4.1 4.75 4.96 3.57 0.8 0.638 11.7 0.33 15.9 2.57 2 0.7 22.3 0.32 5.25 0.8 4.4 3.91 40.9 22.6 1.98 22.1 18.7 0.62 2.61 0.23 0.28 13.9 22 19.4 5.64 9.32 0.07 0.53 0.2 1.01 8.95 9.68 15.7 20.9 18.5 0.53 0.05 0.75 11.7 0.2 3.8 0.5 20.1 6.7 0.36 0.39 26 3.58 0.18 0.06 11.1 0.58 1.73 18.3 0.15 20 0.12 5.88 0.15 3.6 0.46 9.57 0.15 28.6 0.18 1.2 3.44 16.7 1.13 21.5 0.21 0.83 14.2 0.09 0.5 22.7 16.8 1.22 0.14 0.3 24.5 28 21 0.48 1.13 25.8 33.5 0.51 60.1 18.5 48.3 1.87 4.26 1.86 1.380.430.18 2.92 0.57 0.24 2.97 0.44 0.18 0.63 0.48 0.19 0.54 0.32 0.11 0.53 0.37 0.12 0.13 0.46 0.03 0.14 0.03 1.18 0.15 0.04 0.77 0.09 0.02 0.64 0.17 1.62 0.04 0.49 0.16 0.02 0.24 0.1 0.01 0.16 0.27 0.05 0.88 0.31 0.05 0.08 0.01 0.34 0.12 0.01 0.14 0.02 0.09 0.02 16.6 20.1 17 17.1 10.7 11.8 12.1 12.2 12.3 7.12 13.8 15.4 5.7 17 26.6 8.35 9.14 14.4 18.736.1 21.2 41.3 19.8 33.7 17 33.9 10.7 22 13.6 25.5 13.1 27.9 13.6 29.1 14.8 31 8.21 16.9 35.9 51.3 38.2 55.5 31.9 40.5 31.4 57.7 60.7 109 31.7 45 38.3 49.8 64.7 84.2 45.5 53.8 69.0015.5 65.1 16.5 67.04 15.34 66.89 16.03 68.52 16.94 68.37 16.92 77.26 11.29 75.97 11.7 75.7 12.42 77.9 11.23 76.2 12.7 76.25 12.64 76.88 12.44 73.2 13 71.68 14.17 79.09 11.62 77 12.24 76.75 12.15 76.91 12.41 Grano 100 100.3 102.2 102.2 101.6 101.8 99.71 99.72 99.85 99.78 100 100.1 99.8 99.6 100.9 100.5 100.0 99.7 99.7 718 923 419 680 544 369 72.7 82.2 117 71.1 86.8 49.5 22 129 92.9 8.87 4.78 14 diorite P 3 3 5 O 2 2 O O # O 2 O 2 2 2 2 Table 2. (Continued). Deposit Sample A2-7-5 Rock SiO Al Fe FeO MgO CaO Na K MnO TiO P Loi Total Mg A.R. Rb Sr Y Nb Cs Ba La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Ta Pb Th U Zr Hf Data sources: 1674 P.Shen et al.

Figure 11. Classiﬁcation diagrams of samples analysed from the ore-bearing rocks studied. (A) total alkalis versus silica; (B) SiO2 versus # K2O; (C) SiO2 versus A.R., A.R. = (Al2O3 + CaO + Na2O + K2O)/(Al2O3 + CaO − Na2O − K2O); (D) SiO2 versus Mg .(E),(F) discrimination diagrams of I- and A-type granitoids (Whalen et al. 1987).

Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 Note: FG, M + I + S-type fractional granite; OGT, non-fractional M + I + S-type granite; I, fractional I-type granite; S, fractional S-type granite.

deposits and East Kounrad, Zhanet, and Akshatau W-Mo coherent chondrite-normalized (Nakamura 1974) REE pat- deposits are also listed in Table 2. terns, characterized by relative enrichment of light rare The loss on ignition (LOI) for the intrusive rocks in earth elements (LREE) without Eu anomalies (Figure 12). this study ranges from 0.26 to 6.87 wt.%. All major oxides They also have similar E-MORB-normalized (Sun and were LOI-free normalized before petrogenetic interpreta- McDonough 1989) trace element patterns, characterized tion. The ore-bearing rocks from the porphyry Cu deposits by a negative Nb anomaly and a positive Sr anomaly, show a relatively large compositional variation, with SiO2 and enrichment in large ion lithophile elements (LILE) contents ranging from 55.68 to 69.00 wt.%, straddling (Figure 12). Both the REE pattern and spider variation from diorite to granodiorite (Table 2; Figure 11A). They diagram are comparable with those of adakites from the show variable K2O contents (0.37–4.29 wt.%) and low Austral Volcanic Zone, which are believed to be derived and variable A.R. values (1.49–2.98), with calc-alkaline from partial melting of the subducted oceanic crust (Stern characteristics (Figures 11B and 11C). All samples exhibit and Kilian 1996; Figure 12). International Geology Review 1675 Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013

Figure 12. Chondrite normalized (Nakamura 1974) REE distribution and patterns of trace elements normalized (Sun and McDonough 1989) to E-MORB for ore-bearing granitoids from porphyry Cu deposits. 1676 P.Shen et al. Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013

Figure 13. Chondrite normalized (Nakamura 1974) REE distribution and patterns of trace elements normalized (Sun and McDonough 1989) to E-MORB for ore-bearing granites from quartz vein-greisen W-Mo deposits. International Geology Review 1677

The ore-bearing granites in the quartz vein- porphyry are 313.0 ± 2.2 and 312.3 ± 2.2 Ma, respectively greisen W-Mo or Mo deposits have the highest SiO2 (Shen et al. 2012b). Molybdenites formed in the main (71.68–79.09 wt.%), K2O (4.25–5.99 wt.%), and stage yielded a Re-Os mean model age of 312.4 ± 1.8 Ma A.R. values (3.56–5.98) and the lowest MgO con- (Shen et al. 2012b). Therefore, a porphyry-type Cu min- tents (0.10–0.51 wt.%) among samples of this study eralization event occurred in the late Carboniferous in the (Figures 11A–D). They display alkaline and Fe enrichment southern West Junggar ore belt. characteristics and show an evolutionary trend different The SHARMP zircon U-Pb age of the ore-bearing from that of ore-bearing granitoids in the porphyry Cu porphyry is 327.3 ± 2.1 Ma for the Kounrad porphyry deposits. Granites show LREE enrichment and sub- Cu deposit (Li et al. 2012a). The SHARMP zircon age horizontal HREE patterns, with pronounced negative Eu on granodiorite is 327.5 ± 1.9 Ma (Li et al. 2012a), anomalies (Figure 13). Compared with the ore-bearing and SIMS yielded zircon ages from quartz diorite of granitoids in the Cu deposits, granites have the lowest Sr 328.1 ± 2.1 Ma (Cao et al. 2012) for the Aktogai content (average 59 ppm) and Sr:Y ratios (average 3.78). deposit. The SHARMP zircon U-Pb age of the ore- The E-MORB normalized trace element variation diagram bearing porphyry is 316.3 ± 0.8 Ma for the Borly deposit shows bumpy distribution patterns with pronounced (Chen, unpublished), and the Re-Os mean model age troughs at Nb, Sr, Eu, and Ti (Figure 13). is 315.9 Ma for the Borly porphyry Cu deposit (Chen et al. 2010a). Therefore, a porphyry-type Cu mineralization event occurred in the Carboniferous in the North Balkhash 4.2.3. Nd isotopes ore belt. Measured and initial (back-calculated to 310 Ma) isotopic ratios are reported in Table 3. Nd isotopic analyses for the ore-bearing intrusions from the Balkhash ore belt in 5.1.2. Greisen W-Mo mineralization Kazakhstan are also given in Table 3. All samples from ore- In this study, the average model age of molybdenites is bearing stocks in Suyunhe and Baogutu intrusions show a 300.7 Ma for the Suyunhe W-Mo deposit in the south- limited range in their 143Nd/144Nd ratios (Table 3). ern West Junggar. The zircon U-Pb age of the ore-bearing The ore-bearing intrusions in the eastern part of the porphyry is 302 Ma for the Hongyuan Mo deposit, and the North Balkhash and the southern West Junggar ore belts molybdenite Re-Os age is 294.6 Ma (Li et al. 2012b). show uniform high εNd(t) values (+4.45 to +5.94), except The zircon U-Pb age of the ore-bearing porphyry is ± for one at +2.86. Their Nd model ages are very young TDM 299.7 2.7 Ma for the East Kounrad deposit (Cao et al. (403–671 Ma; Table 3). Although the ore-bearing rocks 2012), 306 ± 1Ma(Liet al. 2012a) for the Akshatau from the porphyry Cu deposits and quartz vein-greisen deposit, and 304 ± 4Ma(Liet al. 2012a) for the Zhanet W-Mo deposits are different chemically (Figure 11), they deposit. The molybdenite Re-Os age is 298.0 Ma for the show little variation in isotopic composition (Figure 14A). East Kounrad W-Mo deposit, 295.0 Ma for the Zhanet Mo Ore-bearing rocks from the Cu and W-Mo deposits in deposit, and 289.3 Ma for the Akshatau deposit (Chen et al. the western part of the North Balkhash ore belt show 2010a). slightly varied and low εNd(t) values, ranging from – Based on the available data, two epochs of ore forma- 3.03 to +1.83 except for one at +2.56. Their Nd model tion in the North Balkhash and the southern West Junggar ages are old (TDM = 828–1170 Ma, except for two younger ore belts can be recognized: Carboniferous (328–312 Ma) at 572 and 658 Ma; Table 3). and early Permian (289–300 Ma).

5.2. Petrogenesis

Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 5. Discussion 5.1. Metallogenic ages The geochemical data do not deﬁne a single evolutionary trend for the Carboniferous and Permian ore-bearing rocks For comparison, all U-Pb zircon ages of the ore-bearing from the North Balkhash to the southern West Junggar intrusions and Re-Os ages of molybdenites from the North (Figures 11–13). Moreover, these rocks have different SiO Balkhash metallogenic belt in Kazakhstan and the south- 2 contents but possess similar La/Lu ratios (Figure 15), ern West Junggar metallogenic belt in China are listed in which is not consistent with differentiation of the same Table 4. parental magma. Therefore, these rocks were not derived from fractional crystallization of the same parental magma. 5.1.1. Porphyry Cu mineralization The Baogutu complex in southern West Junggar consists of main-stage diorites and minor late-stage diorite por- 5.2.1. Petrogenesis of the Carboniferous granitoids phyries. Secondary ion mass spectrometry (SIMS) zircon Experimental studies demonstrate that Mg# is a useful U-Pb ages of the main-stage diorites and late-stage diorite index in discriminating melts purely derived from the crust 1678 P.Shen et al. ) ) ) ) ) (2000) (2000) (2000) (2000) (2000) (2000) (2000) (2000) (2000) ) ) ) ) ) ) ) ) ) ) ) ) ) 2008 ( 2009 2009 2009 2009 ( ( ( ( 2012 2012 2012 2012 2012 2012 2012 2012 2012 2012 2012 2012 2012 et al. et al. et al. et al. et al. et al. et al. et al. et al. ( ( ( ( ( ( ( ( ( ( ( ( ( et al. et al. et al. et al. et al. et al. et al. et al. et al. et al. et al. et al. et al. et al. et al. et al. et al. et al. (Ma) Data sources 1160 Liu DM 0.07 10900.09 Liu 1040 Liu 1.110.810.75 1080 1170 658 Liu Liu Heinhorst 0.530.72 1020 828 Liu Heinhorst 3.03 1010 Heinhorst 0.46 1150 Liu 3.393.74 544 525 This study This study 5.51 540 Liu 5.535.44 671 661 Liu Liu 5.584.45 498 603 Heinhorst Heinhorst 5.41 508 Heinhorst 2.86 672 Heinhorst 5.94 403 Heinhorst 5.3 600 Kröner 4.31 522 Shen 4.86 525 Shen 4.42 537 Shen 6.014.065.851.83 618 503 457 1020 Shen This study This study Liu 1.62 572 Heinhorst 1.57 999 Liu 2.56 992 Liu 1.06 Nd(t) T − − − − − ε 5 5 5 8 8 9 9 (ppm) 15 10 10 14 15 10 10 11 10 11 13 12 15 10 σ 2 ± Nd 144 / Nd 143 2 SiO 7776.75 0.512472 0.51229 64.48 0.512257 69.61 0.512419 65.94 0.512502 76.91 0.512097 75.9775.7 0.512812 0.51283 64.27 0.512815 61.05 0.51248 69.72 0.512529 68.52 0.512399 68.37 0.512556 73.35 0.512854 58.95 0.51285 62.05 0.51288 59.98 0.51286 59.9257.1357.84 0.51294 76.25 0.51258 0.51261 0.512509 76.88 0.512341 79.09 0.512529 70.33 0.512424 Rocks Granodiorite Leucogranite Leucogranite Alkali granite Alkali granite Porphyritic Granodiorite 64.1 0.512538 Granodiorite Granite Porphyry stock Granophyre Diorite Quartz diorite Diorite Diorite Aplite Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 Sample Xh080912-9(2)Xh080912-9(3) Granodiorite porphyry Granodiorite 66.51 0.512435 Xh080915-5(3) Adamellite porphyry 71.68 0.512526 Xh080915-5(5) Alkali granite Table 3. Nd isotopic data for theDeposit ore-bearing intrusions from the southern West Junggar and NorthKounrad Balkhash ore belts. Kounrad Xh080910-2(1) Xh080910-7(1) Adamellite porphyry Quartz diorite porphyry 65.24 63.86 0.512472 0.512512 AkshatauAkshatauAkshatau Xh080914-10(1) Xh080914-10(2) AqsK9 Alkali granite Granodiorite Kounrad KoG25 Borly Akshatau AQSG3 Borly Aktogai Xh080919-4(1) Quartz diorite SuyunheSuyunhe ZK03-215 ZK03-221 Aktogai Xh080919-5(4) Granodiorite porphyry 67.04 0.512731 AktogaiAktogai Xh080919-5(5) AQ1 Adamellite porphyry 66.89 0.512738 Aktogai AQ3 Aktogai AQ4 Aktogai AQ7 Aktogai AQ13 AktogaiBaogutu VE 9 BGT5-1 Baogutu BGT5-2 Baogutu BGT5-3 Baogutu BGT5-4 BaogutuBaogutuEast Kounrad ZK201-616 Xh080910-10(1) ZK202-295 Alkali granite Quartz diorite Diorite East Kounrad KoeK16 Zhanet Zhanet Akshatau Xh080914-9(1) granodiorite International Geology Review 1679

Figure 14. (A) εNd(t) versus SiO2; (B) Nd isotopic evolution and Nd isotope data of the ore-bearing rocks. The early to middle Proterozoic crust is from Hu et al. (2000).

Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 from those involved in the mantle. Melts from basaltic whereas the Aktogai and Baogutu have high and posi- lower crust are characterized by low Mg# (<0.4), whereas tive εNd(t) (+4.45 to +5.94; Table 3), suggesting the those with Mg# >0.4 can only be obtained with a man- involvement of the juvenile lower crust (Rapp and Watson tle component involved (Rapp and Watson 1995). All 1995). ore-bearing rocks from the North Balkhash and the south- The ore-bearing rocks have high Sr:Y ratios (aver- ern West Junggar have relatively high Mg# (0.36–0.75) age = 52), low Y (average = 13 ppm), and high Ba and (Figure 11D; Table 2), indicating the involvement of man- Sr contents (average = 490 and = 613 ppm, respectively), tle components. In detail, the Kounrad and Borly deposits which are comparable to those of modern adakites (Defant have relatively low Mg# (0.36–0.52), while the Baogutu et al. 1991; Figure 16). In detail, the Aktogai intrusion and Aktogai have variable and high Mg# (0.38–0.75), exhibits comparable geochemical characteristics to those indicating more involvement of mantle components. of modern adakites (Figure 16). However, the other intru- The Kounrad and Borly deposits have low and negative sions exhibit some distinct geochemical characteristics. For εNd(t) (–0.46 to +0.72; Table 3), indicating the involve- example, compared with adakites, these intrusions have ment of the old continental crust of Central Kazakhstan, slightly low and variable Sr:Y ratios (Figure 16). They also 1680 P.Shen et al.

Table 4. U-Pb zircon ages of the ore-bearing intrusions and Re-Os ages of molybdenites from the southern West Junggar and North Balkhash ore belts.

Deposits Ore-bearing intrusions U-Pb ages (Ma) Data sources Re-Os ages (Ma) Data sources

Porphyry Cu deposits Baogutu Diorite 313.0 ± 2.2 Shen et al. (2012) 312.4 ± 1.8 Shen et al. (2012) Diorite porphyry 312.3 ± 2.2 Shen et al. (2012) Kounrad Adamellite porphyry 327.3 ± 2.1 Li et al. (2012a) Borly Granodiorite 316.3 ± 0.8 Chen (unpublished) 315.9 Chen et al. (2010) Aktogai Granodiorite 327.5 ± 1.9 Li et al. (2012a) Quartz diorite 328.1 ± 2.1 Cao et al. (2012) porphyry Quartz vein-greisen W-Mo deposits Suyunhe Alkali granite 300.7 ± 4.1 This study Hongyuan Granite 302 Li et al. (2012b) 294.6 Li et al. (2012b) East Kounrad Syenogranite 299.7 ± 2.7 Cao et al. (2012) 298.0 Chen et al. (2010) Akshatau Alkali granite 306 ± 1 Chen (unpublished) 289.3 Chen et al. (2010) Zhanet Adamellite porphyry 304 ± 4 Chen (unpublished) 295.0 Chen et al. (2010)

contain high MgO and low SiO2 contents (Figure 11)rel- In the East Kounrad, Akshatau, and Zhanet in the ative to the adakites (Defant et al. 1991). The above data North Balkhash, the alkali granites have low and negative demonstrate that these intrusions have a genetic affinity εNd(t) (–3.03 to +2.56; Table 3), indicating the signifi- between the typical adakites and diorites occurring in the cant involvement of the old continental crust of Central normal arc. In the Sr:Y versus Y diagram (Defant and Kazakhstan. This conclusion is supported by their Nd Drummond 1993) and the (La:Yb)n versus Ybn diagram model ages ranging from 992 to 1170 Ma, except for two (Defant and Drummond 1990), the translation field from at 572 and 658 Ma (Table 3). adakite to normal arc is plotted (Figure 16). All alkali granites show variable Zr contents but less In the Zr:Nb–Zr diagram, partial melting and frac- variable Zr:Nb ratios, indicating a clear fractional crys- tional crystallization show different evolutionary trends tallization trend (Figure 15B). The pronounced negative (Figure 15B). The ore-bearing rocks in Aktogai and Eu and Sr anomalies (Figure 13) suggest fractionation of Baogutu display trends comparable to those of the partial plagioclase and alkali-feldspar. melting process. The ore-bearing rocks in Kounrad and Based on these results, we propose that the precursor Borly show a transitional evolutionary trend from partial magma of the alkali granite in the southern West Junggar melting to fractional crystallization. was possibly derived from a juvenile lower crust, followed Based on these results, we propose that the melt of the by the fractional crystallization process, and the magma ore-bearing rocks at Aktogai is a product of partial melt- of the alkali granites in the North Balkhash was possi- ing of an oceanic slab, while the melt of the ore-bearing bly derived from a mixture of the old continental crust of rocks at Baogutu could be a product of partial melting of Central Kazakhstan and the juvenile lower crust, followed an oceanic slab and later interaction with the mantle dur- by the fractional crystallization process. ing ascent, whereas the melt of the ore-bearing rocks at Kounrad and Borly is a product of partial melting of an

Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 oceanic slab with the involvement of the old continental crust of Central Kazakhstan during ascent. 5.3. Tectonic setting 5.3.1. The basement nature As the early to middle Proterozoic crust has considerably 5.2.2. Petrogenesis of the Permian granites enriched isotopic composition (εNd(t) ≤ 8; Hu et al. 2000; Permian granites in this study are characterized by alkali Chen and Arakawa 2005), incorporation of even small and Fe enrichment; they are alkali granites. In the Suyunhe amounts of the old continental components in the source (the southern West Junggar), because of their high εNd(t) would markedly change isotopic composition. values (+3.39 to +3.74; Table 3), the alkali granites are Most local geologists in Kazakhstan believe in an considered to have been derived from a juvenile lower ancient continental precursor of Central Kazakhstan crust. This conclusion is supported by their Nd model ages, (‘Kazakhstan micro-continent’) (e.g. Glukhan and Serykh ranging from 525 to 544 Ma (Table 3), which are similar to 1996; Popov 1996). In contrast, Heinhorst et al. (2000) and the age of ophiolites in the West Junggar (Xu et al. 2006; Kröner et al.(2008) interpreted the Central Kazakhstan He et al. 2007). basement as a juvenile continental crust in the Phanerozoic International Geology Review 1681

Figure 15. (A) SiO2 versus La:Lu diagram showing that ore-bearing rocks from the Cu and W-Mo deposits have similar La:Lu ratios; (B) Zr:Nb–Zr diagram showing that ore-bearing granitoids from porphyry Cu deposits are controlled by partial melting, whereas ore-bearing granites from quartz vein-greisen W-Mo deposits are dominated by fractional crystallization. Symbols are the same as in Figure 14.

ε +

Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 based on positive Nd(t) (0 to 5.5). Similarly, some In this study, the available data (Heinhorst et al. 2000; authors (e.g. Wu 1987) propose that the West Junggar Kröner et al. 2008; Shen et al. 2009, 2012b; Tang et al. terrane is a micro-continent with Precambrian basement, 2009; Chen et al. 2010a;Liet al. 2012a, 2012b) and our while others (Feng et al. 1989;Carrollet al. 1990) sug- newly acquired isotopic data for the Carboniferous and gest that it represents trapped Palaeozoic oceanic crust and Permian ore-bearing intrusions in the North Balkhash and arc complexes. Chen and Arakawa (2005) conclude that it the southern West Junggar show variable isotopic signa- should be dominated by juvenile crust in the Palaeozoic tures. The Carboniferous and Permian ore-bearing rocks based on the high εNd(t). from the West Junggar and the eastern part of the North Based on our newly acquired data, together with other Balkhash have very similar positive initial εNd(t) values of available data, we propose that the West Junggar and the +2to+6 and depleted mantle model ages in the range of eastern part of the North Balkhash share the basement of 403–672 Ma. As shown in Figure 14B, they plot between the juvenile crust; in contrast, the basement of the western the boundaries for the juvenile crust and depleted mantle. part of the North Balkhash is Precambrian basement with Therefore, we conclude that the basement of the southern juvenile crust. West Junggar and the eastern North Balkhash should be 1682 P.Shen et al.

Figure 16. (A) Diagram of Sr:Y versus Y (Defant and Drummond 1993); (B) diagram of (La:Yb)n versus Ybn (Defant and Drummond 1990) for ore-bearing granitoids in porphyry Cu deposits. Symbols are the same as in Figure 14.

dominated by juvenile crust formed in the early to middle the intrusive rocks. In the SiO2 versus K2Odiagram Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 Palaeozoic and that Precambrian basement must be very (Figure 11B), samples from the Baogutu plot in low- minor, if any. K tholeiite and medium-K calc-alkaline fields, indicating The Carboniferous and Permian ore-bearing intrusions a transitional character from calc-alkaline to tholeiite. in the western part of the North Balkhash plot in both juve- Calc-alkaline rocks are typical constituents of island arcs, nile and Precambrian crusts (Figure 14B). Contributions whereas tholeiitic rocks may be associated with emerg- from Precambrian crust are remarkable. Therefore, the ing island arcs (e.g. Miyashiro 1974), mid-ocean ridges, basement in the western part of the North Balkhash has and backarc-basin spreading centres (e.g. Gill 1976). The both Precambrian basement and juvenile crust. Baogutu intrusive rocks are enriched moderately in LREE and have E-MORB-like Nb:Yb ratios (Figure 17). Thus it is very likely that the Baogutu dioritic rocks formed 5.3.2. Carboniferous tectonic setting in an immature island arc. All samples from the Aktogai Confirming the rock series to which they belong is very plot in the high-K calc-alkaline field (Figure 11B). They important to help discriminate the tectonic setting of have a transitional character from calc-alkaline to alkaline International Geology Review 1683

Figure 17. Th:Yb–Nb:Yb diagram (Pearce and Peate 1995; Sayit and Goncouglu 2009) for ore-bearing granitoids in porphyry Cu deposits. Symbols are the same as in Figure 14.

(Figures 11C and 11D). Alkaline rocks are typical con- Kounrad, Zhanet, and Akshatao in Balkhash plot in the syn- stituents of mature island arcs. Since the Aktogai intrusive collisional granites and volcanic arc granites fields. These rocks are highly enriched in LREE and have OIB-like geochemical signatures suggest that the granites formed in Nb:Yb ratios (Figure 17), the Aktogai intrusive rocks have an arc–continental collision to post-collisional setting. formed in a mature island arc. In addition, since all rocks from the Baogutu and Aktogai have high εNd(t) (+4.35 to +6.01), the Baogutu and Aktogai intrusive rocks have 6. Geodynamic–metallogenic evolution formed in an inter-oceanic island arc. 6.1. Carboniferous geodynamic–metallogenic event Samples from the Kounrad and Borly plot in high- The Kounrad, Borly, and Aktogai in the North Balkhash K and medium-K calc-alkaline fields (Figure 11B). They and Baogutu in the southern West Junggar are typi- are enriched in LREE and have OIB-like Nb:Yb ratios cal porphyry Cu deposits formed in the Carboniferous (Figure 17). In addition, since they have low and negative (328–312 Ma). They are characterized by strongly εNd(t) (–0.46 to +0.72), the Kounrad and Borly rocks form hydrothermal alteration and widely disseminated vein- in an arc setting with a transitional characteristic from a let mineralization. Their ore-bearing magma is the continental to an inter-oceanic arc. subduction-related calc-alkaline magma with adakite features and formed in the magma arc setting during the Carboniferous. In detail, the Baogutu Cu deposit formed 5.3.3. Permian tectonic setting in an immature island arc and the Aktogai Cu deposit From the late Carboniferous to Permian, the Palaeo-Asian formed in a mature island arc, whereas the Kounrad and Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013 Ocean began to close and the plate collided with the Borly Cu deposits formed in a transitional arc setting. Siberian plate (Xiao et al. 2008, 2009). The Balkhash and Therefore, the southern West Junggar and the eastern part the West Junggar entered the collision stage, giving rise to of the North Balkhash belong to an inter-oceanic island extensive granite magmatism. All samples plot in the high- arc, and the western part of the North Balkhash is a tran- K calc-alkaline field (Figure 11B) and the alkaline field sitional arc from a continental arc to an inter-oceanic arc (Figure 11C), indicating that they are alkali granites. Most during the Carboniferous (Figure 19). Simultaneously with alkali granites plot in the I-type granite field (Figures 11E the intrusion of these adakites, volatile matter in remnant and 11F). The Permian granites show negative Eu anoma- magma became saturated, resulting in micro-stockwork- lies and comparatively high HREE abundances in the REE shaped fracturing of porphyry envelopes and country patterns and negative Sr anomalies in the spidergrams rocks. The super-saline fluids released during the early- (Figure 13). In the Rb versus Y + Nb tectonic discrim- stage magmatic crystallization produced areal dissemi- ination diagram for granites (Figure 18), the granites of nated mineralization in the early stage. Ore fluids generated the Suyunhe in the southern West Junggar fall into the in the late stage produced sulphide-quartz veinlets and post-collisional granites field, while the granites of the East stockworks. 1684 P.Shen et al.

Figure 18. Rb versus Y + Nb diagram (Pearce et al. 1984) for ore-bearing granite in quartz vein-greisen W-Mo deposits. Note: ORG, ocean ridge granites; Post-ColG, post-collisional granites; Syn-ColG, syn-collisional granites; VAG, volcanic arc granites; WPG, within-plate granites. Symbols are the same as in Figure 14. Downloaded by [Institute of Geology and Geophysics ] at 18:10 08 September 2013

Figure 19. Sketch showing the evolution of geodynamic setting and related magma and ore deposits in the West Junggar and North Balkhash. (A), (B) Production of island arc responding to slab subduction and associated calc-alkaline magma and porphyry Cu deposits in the Carboniferous. (C), (D) Accretion of the island arc to the western margin of the Kazakhstan plate in the late Carboniferous (Feng et al. 1989). Following the accretion–collision processes, the alkali granite magma and related quartz vein-greisen W-Mo or Mo deposits form in the early Permian. International Geology Review 1685

6.2. Permian geodynamic–metallogenic event Acknowledgements The East Kounrad, Zhanet, and Akshatao in the North This work was granted by the Innovative Project of the Balkhash and Suyunhe and Hongyuan in the southern West Chinese Academy of Sciences (KZCX-EW-LY02), National International Cooperation in Science and Technology project Junggar are typical quartz vein-greisen W-Mo deposits and (2010DFB23390), National Science Fund (41272109, 40972064, formed in the early Permian (289–300 Ma). They are char- 41230207, 40725009, 41190071, 41190072), and National acterized by greisen alteration and related vein mineraliza- 305 Project (2011BAB06B01). tion. The ore-bearing granitic magma is collision-related alkaline magma. Therefore, during the early Permian, the North Balkhash and the southern West Junggar entered the collision stage, giving rise to extensive alkaline granite References magmatism, causing W and Mo mineralization (Figure 19). Abdulin, A.A., Bespaev, H.A., Daukeev, C.Zh., Miroshnichenko, L.A., and Votsalevskiy, E.S., 1998, Copper deposits of The tectonic transition from Carboniferous subduction to Kazakhstan, reference book: Almaty, Kazakhstan, Ministry Permian collision could be key to the formation of the of Ecology and Natural Resources of the Republic of greisen W-Mo deposits in the North Balkhash and the Kazakhstan, 141 p. southern West Junggar. Abdulin, A.A., Bespaev, H.A., Votsalevsky, E.S., Daukeev, The geodynamic–metallogenic events occurred in the S.Z.H., and Miroshnichenko, L.A., 1996, Map of mineral resources of Kazakstan: Non-ferrous metals, Almaty: North Balkhash and the southern West Junggar terranes Kazakhstan Map Publishing House, scale 1:2000000. like the Lachlan fold belt of Australia and the Appalachian BGMRXUAR (Bureau of Geology and Mineral Resources orogen of North America (Blevin and Chappell 1995; of Xinjiang Uygur Autonomous Region), 1993, Regional Samson et al. 1995). 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