Journal of Geosciences, 59 (2014), 255–274

DOI: 10.3190/jgeosci.173

Review paper

Mid–Late Paleozoic metallogenesis and evolution of the Chinese
Altai and East Junggar Orogenic Belt, NW China, Central Asia
Chunming Han1*, Wenjiao Xiao2,1, Guochun Zhao3, Benxun Su1, 3, Patrick Asamoah
Sakyi4, Songjian Ao1, Bo Wan1, Jien Zhang1, Zhiyong Zhang1, Zhongmei WANG1Key Laboratory of Mineral Resources, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China;
cm-han@mail.iggcas.ac.cn
2
Xinjiang Research Center for Mineral Resources, Xinjiang Institute of Ecology and Geography, Chinese Academy of Sciences, Urumqi
830011, China
3
Department of Earth Sciences, The University of Hong Kong, Pokfulam Road, Hong Kong, China
4
Department of Earth Science, University of Ghana, P.O. Box LG 58, Legon-Accra, Ghana* Corresponding author
1

The Chinese Altai–East Junggar collage in southern Altaids is one of the largest and most important metallogenic provinces in China. It is composed of five major types of Middle to Late Paleozoic metal deposits: (1) VMS Cu–Pb–Zn, (2)porphyry Cu–Au, (3) magmatic Cu–Ni-sulfide, (4) skarn Cu–Mo–Fe and (5) orogenic Au. Tectonically, the developmentof these metal deposits was closely associated with accretionary and convergent processes that occurred along the southern
margin of the Central Asian Orogenic Belt (CAOB). The formation of the deposits involved three main stages, briefly
described as follows: (i) Those formed during extensional back-arc volcanism along the Paleozoic active margin of the
CAOB. They are Late Devonian to Early Carboniferous polymetallic volcanogenic massive sulfide deposits, together
with some broadly contemporaneous Fe–Cu skarns, located in the accreted Qiongkuer-Talate Terrane in the western
Altai; (ii) Carboniferous to Permian terrane accretion and arc magmatism, resulting in widespread metalliferous ores ofdifferent types such as copper-bearing porphyries and Alaskan-type Cu–Ni–PGE zoned ultramafic bodies developed inarcs in the Buerjin-Ertai and Erqis terranes, and Cu–Fe skarns formed in the Erqis flysch basin; (iii) Continuing accretionin the Permian leading to the development of the Dulate arc in the southern Altai associated with the formation of Cu–Mo
skarns and orogenic-type gold vein systems. The Chinese Altai–East Junggar collage typically demonstrates the various
classic metalliferous ores formed during the processes of subduction-accretion and arc generation.
Keywords: Chinese Altai, East Junggar, Central Asian Orogenic Belt, Mid–Late Paleozoic, metallogenesis
Received: 16 August 2013; accepted: 24 June 2014; handling editor: O. Gerel

1. Introduction
The Chinese Altai–East Junggar collage is one of thelongest mountain chains in the Central Asian Orogenic
Belt (CAOB) (Şengör et al. 1993, 1996; Buslov et al.
2001, 2004; Windley et al. 2002, 2007; Jahn et al.
2004; Safonova et al. 2011; Kruk et al. 2011) that extends NW–SE for 2,500 km from eastern Kazakhstan
via northern Xinjiang in China to western Mongolia(Fig. 1). It is located between the Sayan and associatedbelts to the north (Federovskii et al. 1995; Xiao et al.
2004) and the Junggar Belt to the south (Zhao ZH etal. 1993; Wang JB et al. 2003). During the past fifty
years many geological and ore-deposit investigations
have led to the recognition of many Paleozoic orogenic
gold, VMS (Cu–Zn, Pb–Zn), skarn (Cu–Mo–Au–Ag)
and Alaskan-type zoned mafic–ultramafic (Cu–Ni–
PGE) mineral deposits, as well as one of the world’s
largest pegmatite-type rare-metal deposits (Rui et al.
2002; Goldfarb et al. 2003; Yakubchuk et al. 2003;
Mao et al. 2008; Sun et al. 2008). As a result, the Altai

has become a world-class metallogenic ore province(Goldfarb et al. 2003).
A better understanding of metallogenesis of thesemineral deposits and their relationships with the tectonic
evolution of the Chinese Altai–East Junggar collage is
now possible because of several detailed studies that havebeen carried out in the past two decades (Wang DH et al.
2002; Wang DH 2003; Wang JB et al. 2003; Wang YW
et al. 2003; Yang FQ et al. 2012, 2013). However, there
have not been extensive reviews in the English language
relating the tectonic evolution of the Chinese Altai–East
Junggar collage to the distribution of different types ofmetal deposits. As a result, the international scientificcommunity poorly understands this tectonic relationship.
In this contribution, we present a detailed overview ofthe geological characteristics of Middle–Late Paleozoic
ore deposits in the Chinese Altai–East Junggar, with emphasis on their alteration, mineralization, geochemistry,metallogenetic timing and associated lithologies, which
will provide insights into the tectonic evolution of theChinese Altai and East Junggar.
www.jgeosci.org

Chunming Han, Wenjiao Xiao, Guochun Zhao, Benxun Su, Patrick Asamoah Sakyi, Songjian Ao, Bo Wan, Jien Zhang, Zhiyong Zhang, Zhongmei Wang

super-terranes in the Cordilleran Orogen of NW America(Şengör et al. 1996; Goldfarb et al. 2003). On the basis of
A large number of terranes were amalgamated to thestratigraphy, metamorphism, mineralization, deformation
Siberian Craton since the Neoproterozoic (Şengör et al.
patterns and age relations, six distinct terranes have been
1993, 1996; Rui et al. 2002), and during the Paleozoic therecognized in the Chinese Altai–East Junggar (Windley
Altai evolved by both northerly- and southerly-directed
et al. 2002) (Fig. 1; Tab. 1).
subductions (Xiao et al. 2004; Zhang ZC et al. 2005).
The Hanasi Terrane (also called “Kanasi”) (Fig. 1a)
The allochthonous terranes range from Neoproterozoic
in northernmost Xinjiang consists of the Neoproterozoic
to Early Carboniferous and mainly consist of island arcs,
to Mid-Ordovician fossiliferous Habahe Grp. and Lateaccretionary wedges, and ophiolites accreted during
Ordovician Baihaba Fm. that were metamorphosed atlong-lived Paleozoic compressional tectonics that was
sub-greenschist facies conditions (Windley et al. 2002).
followed by important sinistral faulting occurring mainly
The Habahe Grp. comprises sandstone, siltstone, shale,at 290–280 Ma (Windley et al. 2002; Laurent-Charvet
marble and chert, while the Baihaba Fm. consists of
et al. 2002, 2003; Buslov et al. 2004; Xiao et al. 2004;
shale, limestone, tuff, granite-porphyry, chert, andesite,
Briggs et al. 2007). These terranes are similar to theandesitic agglomerate and andesitic breccia. The Baihaba
Fm. is considered to have had a source in acontinental-margin andesitic volcanic arc, havTab. 1 Significant mineral occurrences in the Chinese Altai Mts.
ing been deposited in a fore-arc environment
No. NameType
Host terraneOre metals(Windley et al. 2002; Goldfarb et al. 2003). The
Middle to Late Devonian
plutons in the Hanasi Terrane are mainly biotite
1
AsheleVMS
QA
Cu–Zn
and two-mica granites that are undated, except
2
Kaiyinbulake
VMS
CA
Cu–Zn
for the Hanas Lake and Halong-Balisi granites
3
QiaxiaVMS
QA
Fe–Cu
that yielded whole-rock Rb–Sr isochron ages
4
Tiemuerte
VMS
QA
Cu–Pb–Znof 346 ± 5 to 404 ± 3 Ma (Liu W 1993) and the5
Hongdun
VMS
CA
Pb–Zn
Hanasi granite with a whole-rock Sm–Nd iso6
MengkuaiVMS
QA
Cu–Pb–Znchron age of 390 ± 2 Ma (Zhao ZH et al. 1993).
7
Abagong
VMS
QA
Fe–P
8
KumasuVMS
NA
Pb–Zn
The Nuoerte Terrane in northeastern Altai
9
Ahsemlesayi?
VMS
NA
Pb–Zn
contains the Upper Devonian Mangdaiqia Fm.
10
DaqiaoVMS
QA
Cu–Pb–Zncomprising intermediate volcanic rocks, shale,
11
Akeharen
VMS
QA
Pb–Zn
siltstone, greywacke and limestone, and the12
Keketale
VMS
QA
Pb–Zn
Lower Carboniferous Hongshanzui Fm. that
15
Shaersuoke
VMS
QA
Cu–Pb–Zn–Au
consists of sandstone, slate, limestone andLate Carboniferous to Early Permian
intermediate–felsic volcanic rocks (Zhou et
14Duolanasayi
Orogenic
QA
Au
al. 2000; Windley et al. 2002). Windley et al.
13
Qiaoxiahala
Skarn
PE
Fe–Cu–Au(2002) pointed out that this terrane may repre16
Saidu
Orogenic
QA
Ausent two Mid–Late Devonian to Early Carbon17
Samusongbulake
Orogenic
QA
Au
iferous accreted oceanic arcs which were the18
Sarekuobu
Orogenic
QA
Ausame as those in the Delyun-Saksai sub-unit
19
Hongshanzui
Orogenic
QA
Auof the Kanarhirin-Western Sayan accretionary
20
Aketishikan
OrogenicNA
Auwedge and arc of Şengör et al. (1993).
21
Akexike
OrogenicPE
Au
The Central Altai Terrane is made up of
22
MengkuSkarn
QA
Feabundant granites and some Mid-Ordovician
23
Shaerbulake
OrogenicPE
Au
to Silurian metasediments (Long et al. 2008).
24
Suoerkuduke
Skarn
PE
Cu–Mo
25
Kalatongke
MagmaticPE
Cu–Ni
Two idiomorphic zircons from a rhyodacite
26
Aketasi
OrogenicPE
Au
recorded a mean zircon evaporation Pb–Pb age
27
Laoshankou
Skarn
PE
Fe–Cu–Au
of 505 ± 2 Ma that reflects the time of felsic arc
28
Mareletie
OrogenicPE
Au
volcanism, while the presence of 920–614 Ma
Middle Devonian to Early Carboniferous
xenocrysts that survived intracrustal melting
29
Xileketashihalasu
PorphyryPE
Cu–Au
suggests the development of a continental mag30
Yulekenhalasu
PorphyryPE
Cumatic arc on the southern margin of a Precam31
Xietekehalasu
PorphyryPE
Cubrian micro-continent (Windley et al. 2002).
32
Tuosibasitao
Porphyry
QA
Cu–Fe
Four zircons from an orthogneiss gave a zircon
33
Kalasayi
Porphyry
QA
Cu
evaporation Pb–Pb protolith age of 415 ± 1 Ma
Abbreviations for host terranes (Fig. 1a): HS = Hanasi; NT = Nuoerte; CA = Central(Windley et al. 2002). Metasediments in two
Altai; QA = Qiongluer-Abagong; EQ = Erqis; PE = Puerkin-Ertai

2. Regional geological setting256Tectonic and metallogenic evolution of the Chinese Altai and East Junggar

91°E

89°E

87°E

85°E

Russiaab

Kazakhstan

1

Mongolia

4
3

2

5

Terranes:
1 – Hanasi
2 – Nuoerte
3 – Central Altai
4 – Qiongkuer-Abagong
5 – Erqis
6 – Puerkin-Ertai

49°N

2

14

ang

e

49°N

5

19

15

HabaheLak

6Tuergen-Hongshanzui Fault

1

Zais

China

16
17

Ma

6

4

18

9

22

erk

aku

Irtys

8

• •5

3

7

li F

h Fa

7
10

aul 21t

20

Mengku
11
11
12
12

Fuyu

ult

n

47°N

23

47°N

13

Ae

rm

e

but

l
Fau

• •

25

Fa

ult

• 26
• Fig. 4• • 30
27

29
31
32
33

Junggar Basin
0

85°E

an

tai

t

la
Da

24

28

40 km

91°E

89°E

87°E

Mesozoic–Cenozoic cover

Lower Carboniferous

PermianPlutonic rocks

Mafic–ultramafic rocks

Devonian

Devonian–Carboniferous

Metamorphosed volcanic rocks

Silurian

Magmatic Cu–Ni–PGE

Neoproterozoic–Ordovician

Orogenic gold

Skarn Cu–Mo, Fe–Cu

VMS Fe,Cu and Pb–Zn

Porphyry copper

Fig. 1 Generalized geological map of the Altai Shan, NW China, showing the locations of important mines. The insert, after Windley et al. (2002),
shows the distribution of the terranes. Key to mines: VMS Cu–Pb–Zn: 1 = Ashele, 2 = Kaiyinbulake, 3 = Qiaxia, 4 = Tiemuerte, 5 = Hongdun, 6 =Mengkuai, 7 = Talate, 8 = Kumasu, 9 = Ahsemlesayi, 10 = Daqiao, 11 = Akeharen, 12 = Keketale, 13 = Sharesuoke, 22 = Mengku; Orogenic gold:
14 = Duolanasayi, 15 = Qiaoxiahala, 16 = Saidu, 17 = Samusuongbulake, 18 = Sarekuobu, 19 = Hongshanzui, 20 = Aketishikan, 21 = Akexike, 23= Shaerbulake, 26 = Aketasi, 27 = Laoshankou, 28 = Mareletie; Porphyry copper: 29 = Xileketashihalasu, 30 = Yulekenhalasu, 31 = Xietekehalasu,
32 = Tuosibasitao, 33 = Kalsayi; Skarn Cu–Mo: 24 = Suoerkuduke; Magmatic Cu–Ni: 25 = Kalatongke.

locations in this terrane yielded U–Th–total Pb isochronages (CHIME) on monazite of 381 ± 45 Ma, 381 ± 36
Ma and 261 ± 12 Ma, timing the regional metamorphism(Zheng et al. 2007). In the eastern part of the terrane,
major garnet-bearing, post-tectonic anatectic granites arebordered by abundant pegmatites enriched in muscovite,
spodumene, beryl and REE deposits (Fig. 1).

The Qiongkuer-Abagong Terrane contains the Upper Silurian Kumuti Fm. composed of greenschist- toamphibolite-facies schists, the Lower Devonian Kangbutiebao Fm. composed mainly of oceanic arc-type volcanicand pyroclastic rocks, the Lower to Mid-Devonian Ashele
Fm. that contains fossiliferous sediments, basaltic pillow
lavas, hyaloclastites, massive basaltic lavas, lapilli tuffs
257

Chunming Han, Wenjiao Xiao, Guochun Zhao, Benxun Su, Patrick Asamoah Sakyi, Songjian Ao, Bo Wan, Jien Zhang, Zhiyong Zhang, Zhongmei Wangand dacitic lavas (Niu et al. 2006; Yang FQ et al. 2014),
and the Mid-Devonian Altai Fm. of low-grade forearc turbidites. The presence of high-Mg andesites andhigh-Mg adakites in the Ashele Fm. indicates that they
formed in a forearc setting (Niu et al. 1999; Zhang ZC
et al. 2005; Wan et al. 2010). Metasediments from four
locations in the Qiongkuer-Abagong Terrane gave U–Th–
total Pb isochron ages (CHIME) on monazite of 377 ± 30
Ma and 268 ± 10 to 261 ± 20 Ma, reflecting the times ofregional metamorphism (Zheng et al. 2007). Close to thelatter interval are the following ages: a Rb–Sr wholerock age of metavolcanic rocks (285 ± 2 Ma: Windley
et al. 2002 and references therein), a SHRIMP U–Pb
zircon age for orthogneiss (281 ± 3 Ma: Hu et al. 2006),
a Rb–Sr whole-rock age of a granite pluton (256 ± 5 Ma:
Liu W 1993) and a SHRIMP U–Pb zircon age of a posttectonic Lamazhou granitic pluton (276 ± 9 Ma: Wang T
et al. 2005).
The Qiongkuer-Abagong Terrane is dominated by a
Devonian group, which developed along the edge of the
Paleo-Asian Ocean and extends into the southern Urals(Şengör et al. 1993; Dobretsov et al. 1995; Şengör etal. 1996; Buslov et al. 2001; Yakubchuk et al. 2003;
Safonova et al. 2011). The terrane contains many majorore deposits including orogenic-type gold, rare metal
pegmatites, skarns and VMS deposits (Goldfarb et al.
2003; Yakubchuk et al. 2003). The VMS Cu–Zn and
Pb–Zn deposits (e.g. Ashele and Keketale) formed in theforearc setting (Wan et al. 2010), whereas the orogenic
gold deposits (e.g., Saidu and Duodalasayi) developedin association with collision tectonics (Yakubchuk et al.
2003). This terrane is probably equivalent to the Rudnyi
Altai Block in Russian Altai (Buslov et al. 2001, 2004;
D’yachkov et al. 2009; Kruk et al. 2011), and the Turgen
Block in eastern Mongolia (Badarch et al. 2002; Goldfarb et al. 2003).
The Erqis (Irtys, Irtysh) Terrane is situated between
Terrane 4 and the Erqis Fault. The terrane contains
Mid-Ordovician to Silurian schists unconformably
overlain by the Upper Carboniferous Kalaerqis Fm.,
which is also tectonically overlain by the Lower Permian Tesibaerhan Fm. and intruded by Permian granites(Qu and Zhang 1991; Windley et al. 2002; Long et al.
2008). There are different types of mélanges in thisterrane. In the Suoerkuduke area (no. 24 on Fig. 1b),a mélange contains blocks of adakite, basalt, andesite,
diorite, dolerite, lithic tuff, and limestone with Devonian
crinoids. According to Niu et al. (2006), the adakite was
generated by melting of subducted oceanic crust. In the
Shaerbulake area (no. 23 on Fig. 1b), another tectonic
mélange contains blocks of basalt, andesite, volcanic
tuff, dolerite–gabbro, and two types of boninitic rocks,
a massive lava and a pillow lava or breccia. The geochemical features of the boninites suggest that they were258

formed by melting of mildly refractory mantle peridotites fluxed by a slab-derived fluid component (Niu etal. 2006). From the juxtaposition of Devonian volcanic
rocks of different origins such as boninites, adakites,
high- and low-TiO2 basalts within limited area, Niu etal. (2006) concluded that complex accretion and tectonic
processes including duplex thrusting, strike-slip faulting
and serpentinite diapirism were active during Devonian–
Carboniferous convergence and subduction–accretion.
The Erqis Fault is the most prominent terrane-bounding
fault in the Altai, extending for more than 1000 km into
adjacent Kazakhstan and Mongolia (Buslov et al. 2001,
2004; D’yachkov et al. 2009; Kruk et al. 2011). It isdefined by zone of mylonites a 5–10 km wide dated by40
Ar–39Ar method on biotite at 290 ± 2 to 281.4 ± 8.0 Ma(Travin et al. 2001; Laurent-Charvet et al. 2002). The
Erqis Terrane is interpreted to have collided with, andwas accreted below, the southern boundary of Terrane
4, during which the Erqis Fault underwent at least 1000
km sinistral strike-slip movement.
The Puerkin-Ertai Terrane is situated between the
Irtysh and Aermantai faults. It consists of a Devonianisland arc that contains felsic to intermediate basic
lavas and tuffs, andesitic and dacitic porphyries,
and contemporaneous calc-alkaline granitic plutons,
together with shales, sandstones, conglomerates andlimestones (Mei et al. 1993; Yu et al. 1993; Windley
et al. 2002).
The Devonian volcanic rocks enclose many small
blocks of Upper Ordovician limestone. A small early
Carboniferous island arc in the Puerkin-Ertai Terrane
was intruded by several Permian granitic plutons thatare associated with the Suoerkudouke Mo–Cu–Au–Ag
and Qiaoxiahala Fe–Cu–Au deposits (Han BF et al.
1997) and mafic–ultramafic complexes, one of whichhosts the Kalatongke Cu–Ni–PGE deposit (Wang RM
et al. 1991). Yang WP et al. (2005) recognized the
Xileketehalasu porphyry Cu–Au deposit in a Devonianisland arc, for which reason the terrane has become
an important base and a precious metal target area in
Xinjiang.

3. Mineral deposit types and their major
characteristics
The Chinese Altai–East Junggar is remarkable for thediversity of its mineralization. There are more than 220
mines and prospects in an area of c. 110,000 km2 (Wang
DH et al. 2002). Five types of deposits are distinguishedon the basis of their morphology, host rocks, structural
setting, and mineral assemblages (Goldfrab et al. 2003);
their characteristics are summarized in Tab. 2 while thespatial distribution is shown in Fig. 1b.

Tectonic and metallogenic evolution of the Chinese Altai and East Junggar

a

b

800

700
Sectionin Fig. b55'

m a.s.l.

600

0

100 m

500

400

300

200

0

200 m

100
Mid-Devonian Ashele Fm.

Quartz albitophyre

Upper Devonian Qi’ye Fm.

The first member

Copper orebody

Fault

Drill hole

The second member

Quaternary

Exploration line

The third member

Geological boundary

5

5'Fig. 2 Geological map of the Ashele Cu–Zn district (after Wang DH 2003). For location see No. 1 in Fig. 1.

3.1. Mid-Devonian VMS Cu–Pb–Zn
deposits
In the Qiongkuer-Talate Terrane (Fig. 1) there are morethan ten VMS Cu–Pb–Zn deposits at Ashele, Keketale,
Daqiao, Talate, Tiemuerte, Akeharen and Qiaxia (Wang
DH et al. 2002). These deposits are restricted to a NWtrending corridor of VMS Cu–Pb–Zn deposits over 360
km long and 30–70 km wide (Goldfarb et al. 2003);
Ashele and Keketale represent large-scale ore deposits(Wang DH et al. 2002; Han CM et al. 2006).

3.1.1.	Ashele Cu–Zn deposit
The Ashele Cu–Zn deposit is located 30 km NW of Habahe city. It was discovered during a regional geologicalsurvey in 1984 and mining production began in 2004. It isestimated to contain a reserve of 1.08 Mt Cu, 0.43 Mt Zn,
10 t Au, and 860 t Ag, with ore grades averaging 3.42 %Cu, 6.65 % Zn, 0.6 g/t Au and 20–60 g/t Ag (Wang JB etal. 1998; Wang DH 2003).
The main stratigraphic units exposed in the ore district are the Lower–Middle Devonian Ashele Fm. andUpper Devonian Qiye Fm. The ore bodies are mainly
hosted by tuffs and breccias associated with basalt andquartz keratophyre in the hanging wall of a volcanicarc in the Qiye Fm. The principal structures of the ore
district are N–S-trending folds and faults that mostly
post-date the ores. Generally, volcanic edifices formedat the intersections of two faults. Seven mineralization
zones are distributed along N–S-trending faults; thelength of each zone ranges from several meters to a
maximum of 1 km, and the average width is up to tensof meters. Ore body No. 1, the largest in the district,
is a lens-shaped mound, concordant with the folded
bedding, accompanied by a number of small vein-typeore bodies. The main ore body strikes N–S, dipping at
50°E (Fig. 2).
259

260

orogenic

magmatic

Shaerbulake Post-accretion

Post-accretion

Pre-accretion

Pre-accretion

Pre-accretion

Kalatongke

TalateDaqiaoTiemuerte

VMS

VMS

VMS

orogenic

Post-accretion

Saidu

Skarn

orogenic

Pre-accretion

Mengkumagnetite,chalcopyrite,
pyrite, pyrrhotite

Granitic
orthogneiss, biotite–alkali-feldspar
granite, biotite
plagiogranite,
two-mica granite,
hornblendeplagiogranite andquartz diorite
Biotite granite

Basic to intermediate
volcanic breccia, tuff andmarbleTerrigenous detrital rocks
and marine carbonatesof the Early–Middle
Devonian Tuokesalei Grp.

Reserve,
Grade
References

5.328 t Au,
Au mean grade
8.3 g/t

Rui et al.
(2002),
Wang DH et al.
(2002), Liu YL
et al. (2003)

Silicification, pyritization,
110 million t Fe ores, Wang YW
alkali feldspar alteration,
FeO gradeet al. (2003),
carbonation, sericitization,
23.93 % ~ 57.57 %Xu et al. (2010)chloritization, epidotization

Wall-rock alteration

Silicification, pyritization,
pyrite,carbonation, sericitization,
chalcopyrite,
K-feldspar alteration,
kroeberite, galena
chloritization

Metallic minerals

Intrusive rocks

Host rocks

Tuffite, silicolite,siltstone,
limestone, siliceous siltstone
Plagioclase graniteof Early Mid-Devonian
Tuokesalei Grp.

pyrite,Silicification, pyritization,
Rui et al.
chalcopyrite,
10.71 t Au,
carbonation, sericitization,(2002),
kroeberite, galena,
Au
Au grade
K-feldspar alteration,
Wang DH et al.
zinc blende,
2.86 ~ 78.03 g/tchloritization(2002)
magnetitearsenopyrite,
Siltstone, debris tuff,
Silicification, pyritization,
Wang JB etpyrite,5.7 t Au,siltstone, tuff sandstone,
Granite, diorite and chalcopyrite,
carbonation, sericitization,al. (1998),
Au
Au gradesiltstone of Early
granodiorite
K-feldspar alteration,
Wang DH et al.
zinc blende,
1 ~ 16.87 g/t
Carboniferous Nalinkala Fm.
epidotization, chloritization(2002)
kroeberite?,galena, magnetite
No. 1 orebody:
386,000 t of Cu + Ni,
Wang RM et
Sedimentary tuff, tuffaceous
chalcopyrite,
0.18 % Cu,
Diabase–gabbro,
Silicification, chloritization,al. (1991), Yanslate, tuffaceous siltstone,
pyrite, bornite,
0.17 % Ni,
Cu–Niolivine norite, norite
albitization, sericitization,
et al. (2003),
slate of Early Carboniferous
chalcocite,
No. 2 and No. 3
and diorite
epidotization
Han CM et al.
Nanmingshui Fm.
molybdenite
orebodies:(2006)
284,000 t of Cu + Ni,
0.33 % Cu; 0.18 % Ni
chalcopyrite,
Tuff, metatuff, mica-quartz
158,000 t Pb,
Wang JB et al.
pyrite, magnetite,Pb–Zn–Cu- schist, quartz keratophyre, Monzonite, granite
Silicification, sericitization 153,000 t Zn,(1998), Zhangkroeberite, galena,lava breccia
9,000 t Cu
ZX et al. (2012)
zirconSericitized tuff, rhyolite,
800000 t Zn,
magnetite, pyrite, Chloritization,
Wang JB et al.
Cu–Pb–Zn tuffite, jaspilite taconite,
Granite
0.6 % ~3.33 % Zn,
galena, zircon
sericitization, epidotization(2003)
liparite porphyry, marble
0.15 g/t Ag
Granite porphyry
Chlorite–biotite–quartz
Silicification, chloritizaquartz porphyry,magnetite, pyrite,
290000 t Pb + Zn,
Wang JB et al.
Cu–Pb–Zn schist, marble, calcareous
tion, pyritization, sericiquartz-keratophyre, galena, zircon
14000 t Cu
(2003)
siltstonetization
graniteAu

Fe

Genetic type Main metals

Duolanasayi Post-accretion

Tectonic
setting

TypicaldepositTab. 2 Summary of types and main characteristics of metallogenic deposits in the Chinese Altai

Chunming Han, Wenjiao Xiao, Guochun Zhao, Benxun Su, Patrick Asamoah Sakyi, Songjian Ao, Bo Wan, Jien Zhang, Zhiyong Zhang, Zhongmei Wang

Pre-accretion

Pre-accretion

Pre-accretion

Post-accretion orogenic

Post-accretion orogenic

Post-accretion orogenic

Post-accretion orogenic

Keketale

AkeharenKeyinbulake

Aketisikan

Hongshanzui

Akexike

AketasAu

Au

Au
Biotite granite

Early Carboniferous flysch
and mafic/intermediate
volcanic rocks

Middle Devonian basalt,
andesite and basalt tuff

Silicification, K-alternation,
albitization

Silicification
carbonatization,
chloritization, epidotization
chalcopyrite, pyrite

Carbonatization,
silicification, sericitization
Silicification, pyritization,
chalcopyrite,
carbonatization,
pyrite, magnetite
sericitization, chloritization,
epidotization
Silicification, pyritization,
chalcopyrite, pyrite,
sericitization,
Au, galena, zircon
carbonatizationarsenopyrite,
chalcopyrite,
pyrite, zircon,
pyrrhotite,magnetite

Skarn formation,
chalcopyrite, pyrite,
pyritization, silicification,
zircon, pyrrhotite
sericitization, epidotization

galena, zircon,
pyrite2 t of Au,
8.3 g/t Au

0.5–1.7 g/t Au

5.1 t of Au,
4 g/t Au

62600 t of Zn,
2.89 % Pb, 0.13 %Zn, 0.02 ~ 0.10 g/t
Au, 10 g/t Ag
1000 t of Cu,
3000 t of Zn,
1000 t of Pb,
0.22–1.33 % Cu,
1.20–10.78 % Zn

3 Mt Pb + Zn,
3.16 % Zn, 1.51 %Pb, 19.7 g/t Ag,
0.08 % Cu

Reserve,Grade244,160 t of Cu,
12,102 t of Mo,
0.71 % Cu, 0.079 %Mo, 0.23 g/t Au,
3.83 g/t Ag
1.08 Mt Cu, 10 t Au
and 860 t Ag;
3.24 % Cu,
0.6 g/t Au,
20–60 g/t Ag

Diorite, diorite
26 t of Au,
porphyry, quartz
0.98–2.79 g/t Au
diorite porphyry
Early Carboniferous
granodiorite–
chalcopyrite, pyrite, Silicification, carbonatization,
0.5 % Cu,
granophyre,magnetite, bornite, sericitization,
0.39 g/t Au
quartz diorite
molybdenite,prophylitization
porphyry

GraniteNeoproterozoic
to Ordovician phyllite

Devonian andesite, crystal
tuff, tuffaceous siltstone

Biotite granite

Biotite–plagioclase
graniteKyanite–biotite–quartz
Zn–Cu schist, quartzite, quartz
schist, siliceous marble

Devonian phyllite and slate

Rhyolite porphyry

Felsic lava, marble,
Zn–Cu felsic volcanic breccia,
Pb–Zn lava, calc-siltstone, mica
schistAu

Granite porphyry

Silicification, sericitization,
carbonatization,
chloritization, epidotization,
pyritization

Schist, tuffaceous
Pb–Zn metasiltstone, fine-grained
metasandstone, marble

pyrite, pyrrhotite,magnetite, galena
sphalerite,
arsenopyrite,
chalcopyrite,
tetrahedrite,bornite, marcasite

chalcopyrite, pyrite,
Silicification, sericitization,
sphalerite, galena,
pyritization, chloritization,
tennatite, argentite,carbonatization
bornite and cubanite

Wall-rock alteration

Dacite porphyry,
granite porphyry

Metallic minerals

Spilite, spilitic tuff,
Cu–Zn quartz-keratophyretuff, dacite

Intrusive rocks
chalcopyrite, pyrite,
sphalerite, galena,
Skarnization, chloritization,
molybdenite,
epidotization,
marcasite, pyrrhotite serpentinizationand calaverite

Host rocks

Epidote skarn, garnet skarn,
epidote–garnet skarn,
Cu–Mo
Augite diorite
diopside skarn, tuff
sandstone, andesite

MainmetalsXileketehalasu Pre-accretion Porphyry Cu–Au

VMS

VMS

VMS

VMS

Pre-accretion

AsheleSkarn

Genetic
type

Post-accretion

Tectonic
setting

Suoerkuduke

TypicaldepositTab. 2 (Continued)

Yang WP et al.
(2005), Yang etal., (2012)

Goldfarb et al.
(2003), Zhou etal. (2000)

Goldfarb et al.
(2003), Zhou etal. (2000)

Zhou et al.
(2000)

Zhou et al.
(2000)

Wang JB et al.
(1998), Li et al.
(2012)

Wang JB et al.
(2003)

Wang JB et al.
(2003)

Wan et al.
(2010), Yang
FQ et al. (2014)

Wan et al.
(2014)

References

Tectonic and metallogenic evolution of the Chinese Altai and East Junggar

261

Chunming Han, Wenjiao Xiao, Guochun Zhao, Benxun Su, Patrick Asamoah Sakyi, Songjian Ao, Bo Wan, Jien Zhang, Zhiyong Zhang, Zhongmei Wang

The ores exhibit massive, densely disseminated,banded, veinlet-disseminated, and brecciated structures.
The orebody has pronounced vertical zoning, with its
lower part consisting of veined and veinlet-disseminatedores and the middle and upper parts made up of massive ores. From the center of the ore body towards its
margins, the ore types include massive, through banded
to disseminated. The dominant ore is Cu, and associatedmetals include Zn, Ag, Pb, S and Ba, with minor Au, Se,
Cd, Te and Ga.
The ore minerals are dominantly pyrite and chalcopyrite and subordinate sphalerite, galena, tennantite,argentite, bornite and cubanite. Based on crosscutting
relationships, Chen et al. (1996) defined seven stages ofmineralization. Stage 1 is characterized by pyritization,with a representative ore mineral assemblage of quartz +pyrite, which is euhedral-granular and subhedral-granular.
Stage 2 is characterized mainly by a quartz + pyrite +chalcopyrite assemblage that is anhedral-granular. Stage
3 is represented by a quartz + sphalerite + pyrite + chalcopyrite assemblage, while stage 4 is marked by quartz+ sphalerite + pyrite + chalcopyrite + galena + tetrahedrite. Stage 5 consists of pyrite + barite, and stage 6 isrepresented by quartz + pyrite + chalcopyrite + calcite
assemblage that occurs in veins. Stage 7 is marked bysupergene oxidation that gave rise to secondary mineralssuch as malachite + limonite + jarosite + covellite.
The homogenization temperature of fluid inclusions
varies between 168 and 319 ºC and the salinity of fluidinclusions is 1.2–12.4 wt. % NaCl equ. The δD (–142.3

to –39 ‰) and δ18O (–12.3 to –0.3 ‰) values of mineralizing fluids indicate a meteoric origin (Wang DH et al.
2002).

3.1.2.	Keketale Pb–Zn deposit
The Keketale Pb–Zn deposit was discovered in 1986 andis located ~95 km southeast of Altai city (Fig. 1b). It has
reserves of 3 Mt Pb + Zn and 650 t Ag, with ore grades
averaging 3.16 % Zn, 1.51 % Pb, and 19.7 g/t Ag (Wang
JB et al. 1998). In the ore district the dominant Lower
Devonian Kangbutiebao Fm. can be further divided into
lower and upper successions. The lower one consists ofintermediate–felsic lavas, pyroclastic rocks and terrigenous clastic rocks, and the upper one comprises mafic–
felsic volcanic rocks, terrigenous clastic sediments andcarbonates. The deposit is located in the upper successionof the Kangbutiebao Fm.
Many faults in the mineralized area trend predominantly WNW–ESE. The major structure in the area isthe Maizi overturned syncline. Magmatic rocks include
mainly Devonian granites and minor intermediate–basic
dikes and stocks near the fault zone, as well as quartz–(albite) porphyry dikes (Fig. 3).
At the Keketale deposit, a total of 15 ore bodies striking 130–170° and dipping NE at 47–85° have been identified. The gangue minerals present are quartz, plagioclase,muscovite, calcite, diopside, tremolite, almandine, biotite,
hornblende and epidote. The ores have finely granular,
corroded and interstitial textures, and are disseminated,
Zk7–5
Zk7–0
Zk7–7 Zk7–9
Zk7–1
Zk7–2

a

Sectionin Fig. b

Zk7–11

775.27m

0
N

0

80 m

1 km

Middle Devonian sedimentary rocks

Lower Devonian fesic flow

Lower Devonian fragment–bearing tuff

Devonian granite porphyry

Lower Devonian tuff agglomerate

Middle Devonian sedimentary rocks

Pb–Zn ore body

Lower Devonian tuff

Metamorphosed
Lower Devonianrocks
felsic lava
tuff
schistbreccia tuff
calc-siltstonePb–Zn orebody

Drill holebFig. 3 Geological map of the Keketale Pb–Zn deposit (after Wang JB et al. 2003). The Pb–Zn ore bodies are hosted in a metasediment in the Lower
Devonian volcano-sedimentary succession of the Upper Kangbutiebao Fm. For location see No. 12 in Fig. 1.

262

Tectonic and metallogenic evolution of the Chinese Altai and East Junggar

massive, with less common banded, laminated, stockwork
and brecciated structures. Lead grade in the ore bodies
ranges from 0.38 to 4.95 %, with a mean of 1.51 %; Zn
grade varies from 0.40 to 10.74 %, with an average of
3.16 %, while the mean grade of Pb + Zn is 4.67 %. The
Ag grade is commonly less than 40 g/t, but reaching
222 g/t. Based on the mineral assemblages, Wang JB etal. (1998) divided the mineralization into two stages: anearly pyrrhotite + pyrite + sphalerite + galena mineralization and late-stage pyrite + galena veins.

3.2. Middle Devonian–Early Carboniferous
porphyry Cu deposits
Middle Devonian–Early Carboniferous subduction-related tectonics in the Puerkin-Ertai Terrane, immediately
prior to its final docking along the southern margin ofErqis Fault zone, were coincident with a major phaseof porphyry formation. Alkaline plutons within Middle
Devonian tuffs and andesite are associated with porphyry
Cu–Au deposits at Xileketekalasu, Yulekenhalasu, Xietekehalasu, Tuosibasitao and Kalasayi (Fig. 1).
The Xileketekalasu deposit has been best studied andis widely considered to be one of the most economicallysignificant deposits in the Altai Mts. It has reserves ofabout 227685 t of Cu and 7 t of Au based on averageore grades of 0.50 % Cu and 0.39 g/t Au (Yang WP et al.
2005; Fig. 4). The principal ore minerals are chalcopyrite
N
0

400 m

Quaternary

Tuff

Fault

Andesite and basalt

DioriteGeological boundary

Granodiorite porphyry

Granite porphyry

Copper orebody

Fig. 4 Geological map of the Xilekelekalasu Cu–Au district (after Yang
WP et al. 2005). For location see No. 31 in Fig. 1.

and pyrite; the minor ones are bornite, molybdenite andmagnetite. Gangue minerals are mainly quartz, plagioclase, sericite, chlorite, epidote and calcite. The ore has
a medium- to fine-grained, subhedral to anhedral granular
texture, and disseminated and veinlet- disseminated structures. Yang WP et al. (2005) recognized three alteration
zones: potassic, phyllic and propylitic. The mineralized
porphyries have chemical affinities to adakites, whichsuggests that their origin was related to partial meltingof oceanic crust due to northward-dipping subduction of
the Junggar Ocean in the Devonian to Early Carboniferous times.

3.2.1. Late Carboniferous–Early Permianmagmatic Cu–Ni deposits
The Kalatongke mafic–ultramafic intrusion hosts a concentration of massive Cu–Ni-bearing sulfide bodies ina postulated feeder conduit. Indicated and inferred resources of the Kalatongke Cu–Ni sulfide deposit (Fig. 5a)are 1,326,600 t Cu, 777,400 t Ni, more than 4000 t Co,
2.5 t Pt, and 3.4 t Pd (Yan et al. 2003, 2004; Han CM etal. 2007; Mao et al. 2008). The deposit is situated 15 km
south of the Erqis Fault in the Lower Carboniferous
Nanmingshui Fm. of the Puerkin-Ertai Terrane (Fig. 1)(Windley et al. 2002; Goldfarb et al. 2003; Yan et al.
2003).
Sedimentary rocks of the Nanmingshui Fm. are divided into the following three units, numbered from thelowermost upwards (Wang RM et al 1991). Unit 1 in the
SW of the ore district strikes NW–SE, has a maximum
apparent thickness of ~ 200 m and consists of red silty
sandstone, muddy slate, and tuffaceous slate intercalatedwith limestone and siliceous rocks. Unit 2, with a thickness of 300 m, occurs in the central and southwesternparts of the Kalatongke mine, extends NW–SE and dips
to the NE. It includes volcanosedimentary breccia, carbonaceous tuff and andesite and tuffaceous chert (Yan et al.
2003). Unit 3 is located in the central and northern partsof the Kalatongke region, where its outcrop thickness
reaches a maximum of 550 m. It consists of tuffite andcarbonaceous slate with minor limestone, alkali basalt,
basaltic latite and andesite.
In the Kalatongke deposit there are two sets of folds
that strike NW and NWW, with the former being dominant. The southernmost anticline strikes 315°, extendingfor 2500 to 3000 m along strike, with symmetrical limbs
dipping at 40°. There are four sets of faults striking
NW, WNW, EW and NE respectively. The large-scale
NW-striking faults have undergone multiple stages of
movement and the intersections between the NW-striking
and WNW-striking faults are favorable locations for themineralized mafic–ultramafic intrusions (Wang RM et al.
1991; Yan et al. 2003).
263

Chunming Han, Wenjiao Xiao, Guochun Zhao, Benxun Su, Patrick Asamoah Sakyi, Songjian Ao, Bo Wan, Jien Zhang, Zhiyong Zhang, Zhongmei WangAa• • ••

0

ZK34

ZK35

ZK17 ZK36 ZK157 ZK13

B

ZK37

1000

900

100 m

B

800

m a.s.l.

Sectionin Fig. b

A

ZK34

700

600

500

• • ••• • ••b• • • •••

Biotite hornblende norite

Biotite hornblendite

Tuff of Carboniferous
Nanmingshui Fm.

Cu–Ni orebody

Diabase porphyrite

Quartz porphyrite

Sediment-tuff of Carboniferous
Nanmingshui Fm.

Biotite diorite

Fault
ZK34 Drillhole

Fig. 5 Geological map of the Kalatongke Cu–Ni district (after Li et al. 1998). For location see No. 24 in Fig. 1.

Nine mafic–ultramafic intrusions were emplaced into
the Lower Carboniferous Nanmingshui Fm. at the Kalatongke deposit. A well-defined differentiation sequence oflithological zones characterizes many of them. Marginal
diorite grades downwards and inwards, through gabbro andnorite, to a core of pyroxenite and serpentinized harzburgite (Goldfarb et al. 2003; Yan et al. 2003; Mao et al. 2008).
The Kalatongke mine has nine lenticular ore bodies,
the largest of which is No 1. In this ore body, Cu–Ni
sulfide ores are hosted in biotite–hornblende–olivine
norite and biotite–hornblende norite at depths 550–1000
m below the surface (Fig. 5b). The ore body is oxidized
from the surface to depths of more than 40 m, and its orientation is almost parallel to that of the intrusion, which
strikes 334º and dips SE; the upper part dipping at 70 to
90° and the lower part, 0 to 60º (Fig. 5b).
More than 50 ore minerals have been reported fromthe Kalatongke mine (Wang et al. 1991; Han CM et al.
2007) dominated by pyrrhotite, chalcopyrite, pentlandite,violarite, pyrite and magnetite. Associated noble metalbearing minerals are melonite, michenerite, bitepalladite,sperrylite, hessite and electrum. Gangue minerals comprise mainly olivine, pyroxene, plagioclase, hornblende,
biotite, chlorite and serpentinite.
264

The ore minerals are characterized by euhedral,subhedral, anhedral, subhedral–anhedral, porphyritic,
corrosion, relict–replacement, reaction rim and skeletal crystal textures. The ore structures are mainly
massive, vein, veinlet–disseminated, stockworks,
or sparsely disseminated. The mineralization showsa circular zoning pattern, passing from high-grade
massive ore in the center outwards to sub-economic
disseminated ores.
According to the mineral assemblages and crosscutting
relationships, three mineralization stages have been identified (Wang RM et al. 1991). The first assemblage, which
was formed during magmatic crystallization stage, ischaracterized by disseminated ores containing sperrylite,
violarite and magnetite. The second magmatic–hydrothermal stage resulted in the formation of massive and highgrade, vein-like Cu and Ni ores, which have overprinted
the disseminated ores, and contain an assemblage of
Cu- and Ni-bearing minerals, precious metal-bearing
arsenides, tellurides, and tellurobismuthides. The third
stage was marked by supergene oxidation, which led
to the development of a thick gossan and formation of
secondary minerals such as melanterite, chalcanthite andgypsum.

Tectonic and metallogenic evolution of the Chinese Altai and East Junggar

3.3. Late Carboniferous–Early Permian skarn
deposits
Majority of the skarn deposits are of Late Carboniferous–
Early Permian age, and are distributed in the QiongkuerAbagong and Puerkin-Ertai terranes. Skarn-type Fe–Cu
deposits occur in the contact (skarn) zone between intermediate–felsic intrusive rocks and carbonate sediments.
The Mengku skarn-type Fe deposit lies in the middle of
the Qiongkuer-Talate Terrane (Fig. 1a), which is situatedin metamorphosed intermediate–felsic volcanic breccias,
tuffs and marbles. The skarn-type Fe–Cu deposits are
typified by the Qiaoxiahala Fe–Cu–Au deposit in Fuyun
County, with similar deposits occurring at the contact
between subvolcanic (andesite porphyry) to volcanic andpyroclastic rocks. Generally, the mineralization is restricted to bedded skarns, as exemplified by the Suoerkuduke
Cu–Mo deposit in Fuyun County.

3.3.1. Suoerkuduke Cu–Mo deposit
The Suoerkuduke deposit is located c. 114 km SW of
the town of Fuyun. This skarn deposit was discovered in1984 and has been mined since 2004. It is situated in thenorthern part of the East Junggar ore belt, and is hosted in
Mid-Devonian strata of the Beitashan Fm., which locallyconsists of andesite, sandstone and conglomeratic tuffaceous sandstone (Fig. 6). The mine has been estimated40

to contain about 304500 t Cu and 13900 t Mo based on
average ore grades of 0.71 % Cu and 0.06 % Mo (Han
CM et al. 2006). In addition, the grade of precious metals
is 3.83 g/t while that of gold is 0.23 g/t.
The copper ores in the Suoerkuduke deposit can bedivided into two types. The oxidized ores occur near thesurface, typical examples being the oxidized copper ores:
covellite, limonite, malachite, chrysocolla, azurite and hematite. The primary copper and molybdenum ores consistof chalcopyrite and pyrite, with subordinate sphalerite, galena, molybdenite, marcasite and pyrrhotite and minor calaverite, native gold, electrum and malachite. The principal
gangue minerals are epidote, garnet, pyroxene, actinolite,
calcite, chlorite, plagioclase, biotite, quartz, diopside andcarbonate minerals. The ores have anhedral microgranular,anhedral inequigranular and intersertal textures and display
disseminated, veinlet–disseminated and veinlet structures.
Based on field evidence and petrographic observations,four mineralization stages are distinguished: (1) progradeskarn stage (garnet, diopside and epidote), (2) retrograde skarn stage (formation of specularite, magnetite,actinolite, aedelite, plagioclase and meroxene), (3) main
chalcopyrite–molybdenite stage, forming the bulk of theore body (chalcopyrite, molybdenum, pyrrhotine, pyrite,
sphalerite, galena, calcite, quartz, calcite and hematite)and (4) the supergene oxidation stage (formation of secondary minerals such as covellite, limonite, malachite,chrysocolla, azurite and hematite).
ZK4 4

ZK4 5

ZK4 2

ZK4 1

200 m

4
4'

0

50 m

b

a

Quaternary

Andesite

Andesite tuff

Tuffaceous sediment

Andesite porphyrite

Pyroxene andesite

Granitophyre

Porphyrite diorite

Epidote skarn

Acid dike

Fault

Diopside skarn

Garnet skarn

Drill hole

Copper orebody

Fig. 6 Geological map of the Suoerkuduk Cu–Mo deposit (after Li et al. 1998). For location see No. 24 in Fig. 1

265

Chunming Han, Wenjiao Xiao, Guochun Zhao, Benxun Su, Patrick Asamoah Sakyi, Songjian Ao, Bo Wan, Jien Zhang, Zhiyong Zhang, Zhongmei Wang

3.3.2. Qiaoxiahala Fe–Cu–Au deposit

3.3.3. Mengku Fe deposit

This deposit is located c. 23 km SE of the town of Fuyun.
It is hosted in Middle Devonian strata of the Beitashan
Fm. that locally consists of andesite, tuff, sericite phyllite, calcareous-phyllite, volcanic breccia, schistose
limestone and marble (Fig. 7). The deposit contains about
4,620,000 t of Fe ore and 17,600 t of Cu based on averageore grades of 35.05 % Fe and 0.80 % Cu. The deposit
also contains other minor metals such as Co, Ni and Ag(Wang DH et al. 2002).
There are more than ten Fe–Cu ore bodies thatare up to 5000 m long, 10–70 m wide, and >500 m
deep. They are composed of disseminated Fe and Cu
ores, as well as banded and massive Fe ores. The ore
minerals are predominantly magnetite, chalcopyrite,
hematite, iron glance, bornite, pyrrhotite; the gangueminerals are garnet, epidote, chlorite, calcite, quartz
and biotite. Wall-rock alteration related to Fe–Cu
mineralization in the Qiaoxiahala mine mainly includes skarn formation, chloritization, epidotizationand carbonation.

The deposit lies in the central part of the QiongkuerAbagong Terrane (Fig. 1a). It is situated in metamorphosed felsic to intermediate volcanic breccias, tuffs andmarbles of the Lower Devonian Kangbutiebao Fm. The
distribution of the orebodies is controlled by a syncline
on the northeastern limb of the Mengku regional anticline. The Mengku deposit contains twenty ore bodies,
which are mainly distributed in the center of the mining
area; major ore bodies occur in stratiform, stratiform-likeand lenticular bodies. The grade of the ore ranges from23.95 % to 57.57 % of FeO. The dominant ore mineralis magnetite, and gangue minerals include quartz, plagioclase, garnet, diopside and amphibole. Ore structures
range from banded, massive, brecciated, disseminatedto veinlet.
The δ34S values of pyrite are 1.9–14 ‰ and the δ18O
values of magnetite are –3.4 to +0.1 ‰. Fluid inclusions
in quartz show characteristics of medium temperatures(200–400 ℃) and medium salinity (5.8–12.4 wt. % NaClequ.). These data indicate that the sulfur was derived
from the upper mantle, and that some crustal sulfur
was also involved in the oreforming processes (Yang FQ et
al. 2010, 2013).

ab

3.4. Late Carboniferous–   Early Permian   orogenic gold   deposits
Orogenic gold deposits in the
Altai show a clear spatial association with faults (Goldfarb
et al. 2003), marked specificallyby the Tuergen-Hongshanzui,
Erqis and Aermantai faults.

3.4.1. Duolanasayi gold    deposit

Fig. 7b

Devonian phyllite
and graywacke

0

2 km

Hornfels zone
Paleozoic tonalite

266

This deposit is situated 52 km
NW of the town of Habahe. It
was discovered in 1987, andmining began in 1989. The
deposit occurs in a shear zone
cutting the Mid-Devonian
Tuokesalei Fm., which locallyDevonianlimestone

Gold lode

Paleozoic diorite andplagiogranite dyke

Fault

400 m

Fig. 7 Geology of the Duolanasayi orogenic gold deposit, Chinese Altai Shan
(after Rui et al. 2002). For location see
No. 14 in Fig. 1.

Tectonic and metallogenic evolution of the Chinese Altai and East Junggara
ZK190419'

Sectionin Fig. b

19

0

2 km

The
T 1st member of the TuokesaleiFm.: silicalite and sedimentary tuff

Tuokesalei Fm.
sand and conglomerate

The 2nd member of the TuokesaleiFm.: sand, sandy conglomerate

Quartzose sandstone

Plagiogranite

Tertiary

Cataclasite

Phyllonite

Quaternary

Drill holeGold orebody

0

50 m

b

Fault

Fig. 8 Geological map of the Saidu Au deposit (after Wang DH et al. 2002). For location see No. 13 in Fig. 1.

consists of phyllite, graywacke and limestone (Fig. 8).
Several 289 ± 5 Ma (SHRIMP zircon U–Pb dating, Li
et al. 1998) tonalite dikes occur in the area. The deposit
comprises a number of mineralized bodies that occur ina 20×10 km zone between the Maerkakuli and Habahe
N–S trending second-order faults (Rui et al. 2002; Wang
DH et al. 2002). The Au reserve is estimated to be c. 30t with an average of 8.3 g/t (Rui et al. 2002).
The gold ores in the Duolanasayi deposit are grouped
into two types. The oxidized ores are native gold,
limonite, hematite, covellite, digenite, chalcocite, psilomelane, pyrolusite, jarosite, and gypsum. The primaryores occur in disseminated altered rocks and auriferous
quartz–sulfide veins or veinlets. Principal minerals associated with the disseminated altered rocks include native
gold, pyrite, chalcopyrite, pyrrhotite, galena, with minor
molybdenite, magnetite and tetrahedrite. The auriferous
quartz–sulfide vein ores are composed mainly of massive
quartz, and minor albite, ankerite, calcite, chlorite, pyrite,
chalcopyrite, galena, molybdenite, sphalerite and native
gold. The sulfide and gold minerals exhibit disseminated,massive and veinlet structures in quartz fractures.
Wang Z (1991) divided auriferous hydrothermal activity at the Duolanasayi deposit into four stages: (1) early
pyrite–quartz–scheelite, (2) pyrite–chalcopyrite–sphalerite–galena–quartz, (3) quartz–dolomite–calcite, and(4) late quartz–jarosite–limonite–gypsum. Although all

the four stages were involved in the deposition of gold,
the first two are the most important, whereas the fourthstage led to the enrichment of gold in the oxidized zones.
Wang Z (1991) showed that the δ34S composition of
pyrite in the ore in the Duolanasayi deposit ranges from
–8.8 to +1.4 ‰, with a mean of –2.9 ‰, suggesting thatthe sulfur had a deep crustal or upper mantle source, andthat mixing with upper crust was part of the ore-forming
process (Liu YL et al. 2003).

3.4.2. Shaerbulake gold deposit
This deposit is located c. 32 km SW of Fuyun (Fig. 1).
This shear zone-hosted gold deposit was discovered in
1986, but mining commenced in 1989. The deposit ishosted in the Lower Carboniferous Nalinkala Fm., which
consists of phyllite, siltstone, tuffaceous sandy conglomerate and limestone. The ore deposit occurs in a 18 × 2 km
zone along the NW-trending Saerbulake Fault (Wang DH
et al. 2002). It is estimated to contain c. 10 t Au and an
average Au grade of 6 g/t (Rui et al. 2002).
Principal metallic minerals include native gold, electrum, pyrite, arsenopyrite and pyrrhotite. The gangueminerals are quartz, albite, sericite, and ankerite. The
ores are characterized by euhedral, subhedral and pseudomorphic textures, while the structures include dissemination, veinlet-dissemination and brecciation ones. The ore267

Chunming Han, Wenjiao Xiao, Guochun Zhao, Benxun Su, Patrick Asamoah Sakyi, Songjian Ao, Bo Wan, Jien Zhang, Zhiyong Zhang, Zhongmei Wang

bodies are vein-shaped and hosted in NW–SE sheared
alteration zones that strike.
Five mineralization stages can be distinguished (Wang
DH et al. 2002): (1) early quartz–arsenopyrite, (2) pyrite–
quartz, (3) quartz–dolomite–calcite, (4) quartz–albite and(5) late jarosite–limonite–gypsum.

3.4.3. Saidu gold deposit
This deposit is situated NE of Habahe (Fig. 1). It ishosted in the Lower to Middle Devonian Tuokesalei
Fm. that consists of sandstone, limestone and pelite.
The deposit consists of a number of mineralized bodies
occupying an area of 18 × 2 km along the Maerkakuli
Fault (Liu YL et al. 2003). Gold ores are concentrated
in four groups that occur in an area of c. 4 × 1 km (LiuYL et al. 2003).
The Saidu ore bodies include auriferous quartz
veins, altered dikes, and altered clastic rocks. The goldores are divided into two types: oxidized and primary.
The sulfides and oxides include pyrite, chalcopyrite,
pyrrhotite, magnetite, hematite, galena, sphalerite,
marcasite, molybdenite, ilmenite and rutile. Four paragenetic stages can be identified: (1) magnetite–quartz,(2) pyrite–quartz, (3) sulfide–native gold–quartz, and(4) quartz–carbonate.

4. Discussion

4.1. Geochronological data for ore deposits
Based on their geochronological data (Tab. 3), the mineral deposits in the Chinese Altai can be classified into
three groups: (i) pre-accretionary VMS deposits (c. 380–
360 Ma) and porphyry Cu–Mo deposit (c. 370–330 Ma),(ii) syn-to post-accretionary magmatic Cu–Ni deposits
and skarn Cu–Mo deposit (c. 304 Ma) that formed in
Late Carboniferous to Early Permian (c. 305–285 Ma)
and (iii) syn-to post-accretionary orogenic gold lodes(c. 290–280 Ma).
The hanging wall of the principal Ashele orebody (No.
1) is an Ashele Fm. tuff that yielded a concordant zircon
U–Pb age of 387.0 ± 4.2 Ma, whereas the footwall basalt
gave a weighted average 206Pb/238U age of 388.0 ± 3.3 Ma(Yang FQ et al. 2014). The two ages indicate that the
principal orebody of the Ashele Cu–Zn deposit formed
during the Mid-Devonian, at around 388 Ma (Tab. 3).
In the Devonian Ashele Fm., the iron jaspers gave a
Rb–Sr isochron age of 378 ± 39 Ma and a Sm–Nd isochron age of 373 ± 14 Ma (Li HQ et al. 1998). From the
Ashele deposit, the following Rb–Sr isochron ages wereobtained; laminated chalcopyrite (364 ± 15 Ma), pyrite–
quartz veins (302 ± 11 Ma), and tetrahedrite-bearing car268

bonate–quartz veins (255 ± 16 Ma), whereas the blendes
gave Rb–Sr and Sm–Nd isochron ages of 265 ± 8 Ma
and 282 ± 11 Ma respectively (Li HQ et al. 1998; Wang
DH et al. 2002). Taken together, the Ashele VMS Cu–Zn
deposit may have undergone a protracted mineralization
history, although the main phase of mineralization took
place in the Devonian. Hydrothermal alteration in the
Carboniferous–Permian probably modified and upgraded
the deposit.
Sphalerites in the ores of Keketale gave a Sm–Ndisochron age of 373 ± 15 Ma, while Rb–Sr isochron age
dating of the blendes yielded 274 ± 8 Ma (Li HQ et al.
1998). The former represents the mineralization age ofthe Keketale Pb–Zn deposit, whereas the latter reflects
reworking during a late thermal event. This suggeststhat the deposit experienced a protracted or two-stage
thermal history.
SHRIMP U–Pb zircon ages of 381 ± 6 Ma and 375 ± 9
Ma were obtained for a mineralized granodiorite porphyry and Re–Os isochron ages of 378 ± 6 Ma and374 ± 2 Ma for molybdenites from the Xileketashihalasu
porphyry Cu deposit (Zhang ZC et al. 2006; Wu et al.
2008; Yang FQ et al., 2010). Zhao ZF et al. (2009) dated
the Yulekenhalasu porphyritic granite by a LA-ICP-MS
zircon U–Pb method at 381.6 ± 2.5 Ma, for which Yang
FQ et al. (2012) have obtained a molybdenite Re–Os
isochron age of 373.9 ± 2.2 Ma (Tab. 3).
Wang YW et al. (2010) presented a Re–Os isochron
age of 327.1 ± 2.9 Ma for molybdenites of the Xilekuduke, for which Long LL et al. (2010) have publisheda LA-ICP-MS zircon U–Pb age of 329.3 ± 2.3 Ma.
Olivine norite, norite, hybrid norite and diabase–gabbro from the Kalatongke Cu–Ni deposit gave Rb–Sr
isochron ages of 285 ± 16 Ma, 298 ± 23 Ma, 302 ± 32 Ma
and 317 ± 50 Ma respectively (Wang RM et al. 1991).
Similarly, the Cu–Ni-bearing mafic–ultramafic rocks weredated by the SHRIMP U–Pb method on zircon at 287 ± 5
Ma (Han BF et al. 2004). Accordingly, we suggest thatthe emplacement age of the Kalatongke intrusion ranges
between 298 and 285 Ma. In addition, the massive anddensely disseminated sulfide ores from the Kalatongke
Cu–Ni deposit yielded a Sm–Nd isochron age of 281 ± 12
Ma (Li HQ et al. 1998), whilst Re–Os age dating of the
Kalatongke No. 1 deposit gave 305 ± 15 Ma (Han CM
et al. 2007). In summary, these isotopic data indicatethat the Kalatongke mafic–ultramafic intrusion and its
associated Cu–Ni deposit formed in the Late Carboniferous–Early Permian.
In the Suoerkudouke area, altered (pyroxene) andesite,
and its porphyry gave a whole-rock Rb–Sr isochron ageof 288 ± 18 Ma (Li HQ et al. 1998), which is comparable
to a Rb–Sr isochron age of 274.0 ± 1.1 Ma for the andesite(Hu et al. 1993). On the other hand, garnet and epidote in
the ore-bearing skarns in the Suoerkuduke deposit have

Tectonic and metallogenic evolution of the Chinese Altai and East Junggar

Tab. 3 Available geochronological data for ore deposits in the Chinese Altai
Name of deposit
Ashele Cu–Zn
"
"
"
"
"
"
"
"
Keketale Pb–Zn"
Xileketashihalasu Cu"""
Yulekenhalasu Cu"
Xilekuduke Cu–Mo"
Kalatongke Cu–Ni
"
"
"
"
"
Suoerkuduke skarn Cu–Mo"""
Duoalnasayi Au""
Saerbulake Au
Saidu Au"""

Dated minerals/rocks
Tuff
BasaltIron jasper
Iron jasper
Chalcopyrite
Quartz-pyrite
Carbonate-quartz
BlendeBlendeSphalerite
BlendeGranodiorite porphyry
Granodiorite porphyry
Molybdenite
Molybdenite
Porphyrite granite
Molybdenite
Enclaves in granodiorite
Molybdenite
Olivine norite
NoriteHybrid norite
Diabase gabbro
Biotite norite
Cu–Ni ores
SulfidesPorphyry
Andesite
Garnet, epidote
Molybdenite
Quartz, fluid inclusions
Muscovite
Muscovite
GraniteMuscovite
Muscovite
Quartz, fluid inclusions
Quartz, fluid inclusions

a Sm–Nd isochron age of 284.3 ± 3.9 Ma (Li HQ et al.
1998). Recently, Wan et al. (2014) presented a Re–Os
isochron age of 304.7 ± 7.3 Ma for molybdenites of the
Suoerkudouke.
Other geochronological studies have also produced
different ages. For example, Li HQ et al. (1998) reported
Rb–Sr ages of 269 ± 13 Ma for fluid inclusions in mineralized quartz from the Duolanasayi gold deposit andof 306 ± 7 to 272 ± 19 Ma for those from the Saidu gold
deposit. Yan et al. (2004) also obtained an Ar–Ar plateau
age of 292.8 ± 1.0 Ma and an isochron age of 293.1 ± 4.8
Ma for muscovite from the Duolanasayi deposit, and
Ar–Ar plateau age of 289.2 ± 3.1 Ma and isochron ageof 291.3 ± 8.4 Ma for muscovite from the Saidu gold
deposit.

Dating method
LA-ICP-MS zircon U–Pb
LA-ICP-MS zircon U–Pb
Rb–Sr isochron
Sm–Nd isochron
Rb–Sr isochron
Rb–Sr isochron
Rb–Sr isochron
Rb–Sr isochron
Sm–Nd isochron
Sm–Nd isochron
Rb–Sr isochron
SHRIMP zircon U–Pb
SHRIMP zircon U–Pb
Re–Os isochron
Re–Os isochron
LA-ICP-MS zircon U–Pb
Re–Os isochron
LA-ICP-MS zircon U–Pb
Re–Os isochron
Rb–Sr isochron
Rb–Sr isochron
Rb–Sr isochron
Rb–Sr isochron
SHRIMP zircon U–Pb
Sm–Nd isochron
Re–Os isochron
Rb–Sr isochron
Rb–Sr isochron
Sm–Nd isochron
Re–Os isochron
Rb–Sr isochron
Ar–Ar plateau
Ar–Ar isochron
SHRIMP zircon U–Pb
Ar–Ar isochron
Ar–Ar plateau
Rb–Sr isochron
Rb–Sr isochron

Age (Ma)
387.0 ± 4.2
388.0 ± 3.3
378 ± 39373 ± 14364 ± 15302 ± 11255 ± 16265 ± 8282 ± 11373 ± 15274 ± 8381 ± 6375 ± 9378 ± 6374 ± 2381.6 ± 2.5
373.9 ± 2.2
329.3 ± 2.3
327.1 ± 2.9285 ± 16298 ± 23302 ± 32317 ± 50287 ± 5281 ± 12305 ± 15288 ± 18274.0 ± 1.1
284.3 ± 3.9
304.7 ± 7.3
269 ± 13292.8 ± 1.0
293.1 ± 4.8
410 ± 4291.3 ± 8.4
289.2 ± 3.1
306 ± 7272 ± 19

Data sources
Yang FQ et al. (2014)
Yang FQ et al. (2014)
Li HQ et al. (1998)
Li HQ et al. (1998)
Li HQ et al. (1998)
Li HQ et al. (1998)
Li HQ et al. (1998)
Wang DH et al. (2002)
Wang DH et al. (2002)
Li HQ et al. (1998)
Li HQ et al. (1998)
Zhang ZC et al. (2006)
Wu et al. (2008)
Yang FQ et al. (2010)
Wu et al. (2008)
Zhao ZF et al. (2009)
Yang FQ et al. (2012)
Long LL et al. (2010)
Wang YW et al. (2010)
Wang RM et al. (1991)
Wang RM et al. (1991)
Wang RM et al. (1991)
Wang RM et al. (1991)
Han BF et al. (2004)
Li HQ et al. (1998)
Han CM et al. (2007)
Li HQ et al. (1998)
Hu et al. (1993)
Li HQ et al. (1998)
Wan et al. (2014)
Li HQ et al. (1998)
Yan et al. (2004)
Yan et al. (2004)
Liu F et al. (2010)
Yan et al. (2004)
Yan et al. (2004)
Li HQ et al. (1998)
Li HQ et al. (1998)

4.2. Metallogenic evolution of the Chinese
Altai Shan
The Chinese Altai occupies a key position within the Central Asian belts (Hu et al. 2000; Xiao et al. 2004), and its
geodynamic evolution was closely associated with that of
the CAOB. Most terranes were developed by subductionrelated processes and accreted in a southward direction
from the Cambrian (e.g. Habahe Grp.) to the Permian(e.g. Kuerti Fm.). Lateral growth of the southern Chinese
Altai indicates a massive addition of juvenile material to
the Paleozoic crust (Şengör et al. 1993; Xiao et al. 2004).
The Late Carboniferous–Early Permian Chinese Altai
island arc contains subduction-generated adakites andboninites (Xiao et al. 2004) and the presence of Alaskan269

Chunming Han, Wenjiao Xiao, Guochun Zhao, Benxun Su, Patrick Asamoah Sakyi, Songjian Ao, Bo Wan, Jien Zhang, Zhiyong Zhang, Zhongmei Wang

type mafic–ultramafic complexes (Laurent-Charvet et al.
2002; Han CM et al. 2007) suggests that the southern
Altai developed in a subduction–accretion setting in the
Late Carboniferous–Early Permian (Xiao et al. 2004).
The Kalatongke mafic–ultramafic intrusion was previously considered as having formed in a post-orogenic
extensional setting in the Late Carboniferous–Early
Permian (Wang JB et al. 2003). However, the most recent
Re–Os geochronological and geochemical results indicatethat this intrusion, along with the Cu–Ni deposit, wasproduced by subduction–accretion of oceanic crust.
In the southern Altai, southwest-directed rollback andassociated slab-detachment occurred during the Devonian(400 to 370 Ma) in response to a later addition to the collision zone at the accreting continental margin (Fig. 9a;
Xiao et al. 2004). Mafic and alkalic igneous activity associated with different types of mineralization occurred in
the Kelang Basin during this backarc extensional event,which was possibly associated with the upwelling of theasthenosphere (Fig. 9b). Thus the slab rollback not only
triggered the backarc extension but also provided a heatsource for the partial melting that initiated the Middle
Devonian felsic magmatism. The upwelling of the asthenosphere also could have yielded hydrothermal fluidsthat led to the VMS Cu–Pb–Zn mineralization (Fig. 9b),a process analogous to the Pliocene tectonic setting in Fijifollowing the collision of the Ontong Java Plateau with
the Melanesian Arc (Han CM et al. 2006).
In our model, the development of the mineralized granodiorite porphyry complexes was associated with northdipping subduction–accretion, which led to the formationof the southern part the Dulate-Baytag Arc, as evidenced
by the presence of adakites (Yang WP et al. 2005). In the
Middle Devonian–Early Carboniferous, the northwarddipping subduction of an oceanic slab is thought to haveresulted in the formation of a magmatic arc in the southern
Altai and East Junggar. At the leading edge on the upper
plate, these complexes initially experienced adakitic magmatism in response to the partial melting of slab material.
Opening a slab window beneath these complexes could
have led to multiple pulses of magmatism and productionof crustal melts (Thorkelson and Breitsprecher 2005).
Concentrically zoned mafic–ultramafic intrusions,similar to those in the Alaskan-type belts, developed from
Late Carboniferous to Early Permian in the Dulate Arc,
north of the Erqis Terrane. They were accreted to theSiberian continental margin during the earliest Permian
subduction–accretion. The identical ages of the magmatic
Cu–Ni sulfide and Cu–Mo–Fe skarn deposits suggestthat they were all linked to the final stages of terraneaccretion and related subduction magmatism (Xiao et al.
2008; Fig. 9c).
During the Late Carboniferous to Early Permian, theChinese Altai was transformed into a continental magmatic270

arc in which an extensive lode gold mineralization occurred throughout the accreted margin (Fig. 9c). Late Carboniferous to Early Permian subduction-related plutonism
within the Erqis Terrane, the autochthonous rocks occurring in the Puerkin-Ertai Terrane to the south, resulted in
the development of a major gold province in the southern
Altai, and the formation of gold–quartz veins in the Erqis
and Puerkin-Ertai terranes from 305 to 270 Ma (Goldfarb
et al. 2003). The upper greenschist to amphibolite-facies
dehydration reactions were probably responsible for the
production of the appropriate vein-forming fluids.

5. Conclusions
The mineral deposits in the Chinese Altai–East Junggar
can be categorized into five major types: (1) Devonian VMS Cu–Pb–Zn deposits, (2) Early Carboniferous
porphyry-type Cu–Au deposits, (3) Late Carboniferous–
Early Permian Alaskan-type Cu–Ni–PGE sulfide deposits, (4) Late Carboniferous–Early Permian skarn-type
Cu–Mo–Fe deposits and (5) Late Carboniferous to Early
Permian orogenic-type Au deposits.
The presence of VMS Cu–Pb–Zn deposits generally
points to a long-lived subduction–accretion and growthby forearc accretion, following the model of forearc accretion in Japan. The Devonian accretion and associatedslab-tearing probably triggered the slab rollback, crustal
thinning and asthenospheric upwelling, which could haveprovided the heat for mineralization associated with the
VMS Cu–Pb–Zn mineralization.
From the Late Devonian to Early Carboniferous, thenorth-dipping subduction beneath the Dulate Arc led to
the genesis of subduction-related porphyry Cu–Au deposits. From the Late Carboniferous to Early Permian, syn-to
post-accretionary Cu, Ni and Au deposits developed inassociation with a series of subduction, convergent anddelamination events, leading to the formation of Cu, Ni
and Au mineralization restricted to the southern Chinese
Altai.
Acknowledgements. We are indebted to Xianhua Li,
Kezhang Qin and Lianchang Zhang for thoughtful discussions, which improved and initiated many of the ideas inthis paper. We are grateful to Emil Jelínek for his constructive discussions and comments on an early versionof the manuscript, which led to substantial improvementsof the paper. This study was financially supported byfunds from the National Natural Science Foundation
Projects (41190075, 41230207, 41272107), the National
305 Projects (2011BAB06B04–1), the Chinese State 973
projects (2014CB440801, 2007CB411307), and Hong
Kong RGC (7066/07P). This paper is a contribution to
IGCP 592.

Tectonic and metallogenic evolution of the Chinese Altai and East Junggar

A Late Ordovician to SilurianSouthern Angara
Active Margin
v

v
v

SW

Altai-Fuyun
Island ArcNE

Dulate-Baytag
Arc
Kamaili Ocean

Zaisan Oceanv v

TurgenAccretionary
ComplexB Early Devonian to Late Carboniferous
SW

NE
Altai-Fuyun
Southern Angara
Active Margin VMS deposit Island Arc
V V

Dulate-Baytag
Arc

Zaisan OceanV
V V +++ V V
VKamaili Ocean

V •
V •

•

Hydrotherma lflui ds

V

V
V

V

V

Porphyry Cu–Au
depositVV
V V

Potentital
slab melting zone

Upwelling ofasthenosphere

C Late Carboniferous to Early Permian
NE

SW

Dulate-Baytag
ArcSouthern Angara
Active Margin Orogenic Au deposit

Skarn Cu–Mo deposit
Kamaili Ocean

Alaskan-type zoned pluton
and Cu–Ni deposit

mantle upwelling

V

V
V

Arc

+

+
+

GraniteContinental crust

Accretionary complex

Oceanic crust

Fig. 9 Schematic diagrams showing the late Paleozoic evolution and the formation of metal deposits in the Chinese Altai (after Xiao et al. 2004;
Han CM et al. 2006). See text for discussion.

References
Badarch G, Cunningham WD, Windley BF (2002) A new
terrane subdivision for Mongolia: implications for the
Phanerozoic crustal growth of Central Asia. J Asian
Earth Sci 21: 87–110
Briggs SM, Yin A, Manning CE, Chen ZL, Wang XF,
Grove M (2007) Late Paleozoic tectonic history of theErtix Fault in the Chinese Altai and its implications forthe development of the Central Asian Orogenic System.
Geo Soc Am Bull 119: 944–960
Buslov MM, Saphonova IY, Watanabe T, Obut OT, Fujiwara Y, Iwata K, Semakov NN, Sugai Y, Smirnova
LV, Kazansky AY, Itaya T (2001) Evolution of the
Paleo-Asian Ocean (Altai-Sayan, Central Asia) and collision of possible Gondwana-derived terranes with the271

Chunming Han, Wenjiao Xiao, Guochun Zhao, Benxun Su, Patrick Asamoah Sakyi, Songjian Ao, Bo Wan, Jien Zhang, Zhiyong Zhang, Zhongmei Wang

southern marginal part of the Siberian continent. Geosci
J 5: 203–224
Buslov MM, Watanabe T, Fujiwara Y, Iwata K, Smirnova
LV, Safonova IY, Semakov NN, Kiryanova AP (2004)
Late Paleozoic faults of the Altai region, Central Asia:
tectonic pattern and model of formation. J Asian EarthSci 23: 655–671
Chen YC, Ye QT, Feng J, Mu CL, Zhou LR, Wang QM,
Huang GZ, Zhuang DZ, Ren BC (1996) Ore-forming
Conditions and Metallogenic Prognosis of the Ashele
Copper–Zinc Metallogenic Belt, Xinjiang, China. Geological Publishing House, Beijing, pp 1–330 (in Chinese)
Dobretsov NL, Berzin NA, Buslov MM (1995) Opening
and tectonic evolution of the Paleo-Asian Ocean. Int
Geol Rev 37: 335–360
D’yachkov BA, Titov DV, Sapargaliev EM (2009) Ore
belts of the Greater Altai and their ore resource potential.
Geol Ore Depos 51: 197–211
Fedorovskii VS, Khain EV, Vladimirov AG, KarGopolovSA, Gibsher AS, Izokh AE (1995) Tectonics, metamorphism, and magmatism of collisional zones of the Central
Asian Caledonides. Geotectonics 29: 193–212
Goldfarb RJ, Mao JW, Seltmann R, Wang DH, Xiao WJ,
Hart C (2003) Tectonic and metallogenic evolution of
the Altai Shan, Northern Xinjiang Uygur Autonomous
region, Northwestern China. In: Mao JW, Goldfarb RJ,
Seltmann R, Wang DH, Xiao WJ, Hart C (eds) Tectonic
Evolution and Metallogeny of the Chinese Altai and Tianshan. Proceeding Volume of the International Symposiumof the IGCP-473 Project in Urumqi, pp 17–30
Han BF, Wang SG, Jahn BM, Hong DW, Kagami H, Sun
YL (1997) Depleted-mantle source for the Ulungur River
A-type granites from North Xinjiang, China: geochemistry and Nd–Sr isotopic evidence, and implications forPhanerozoic crustal growth. Chem Geol 138: 135–159
Han BF, Ji JQ, Song B, Chen LH, Li ZH (2004) SHRIMP
zircon U–Pb ages of Kalatongke No. 1 and Huangshandong Cu–Ni-bearing mafic–ultramafic complexes, North
Xinjiang and geological implications. China Sci Bull 49:
2324–2328 (in Chinese)
Han CM, Xiao WJ, Zhao GC, Mao JW, Li SZ, Yan Z,
Mao QG (2006) Major types, characteristics and geodynamic mechanism of Upper Paleozoic copper deposits
in northern Xinjiang, northwestern China. Ore Geol Rev
28: 308–328
Han CM, Xiao WJ, Zhao GC, Qu WJ, Du AD (2007) Re–Os
dating of the Kalatongke Cu–Ni deposit, Altai Shan, NW
China, and resulting geodynamic implications. Ore Geol
Rev 32: 452–468
Hu AQ, Zhang GX, Li QX, Fan SK, Zhang SF (1993)
Isotope geochemistry and crustal evolution of Northern
Xinjiang. In: Tu GZ (ed) New Improvement of Gold
Geosciences in Northern Xinjiang. Beijing Science Publishing House, Beijing, pp 27–37 (in Chinese)272

Hu AQ, Jahn BM, Zhang GX (2000) Crustal evolution andPhanerozoic crustal growth in northern Xinjiang: Nd
isotopic evidence. Part I. Isotopic characterization of
basement rocks. Tectonophysics 328: 15–51
Hu AQ, Wei GJ, Deng WF, Chen LL (2006) SHRIMP zircon
U–Pb dating and its significance for gneisses from thesoutheast area to Qinghe Country in the Altai, China. Acta
Petrol Sin 22: 1–10 (in Chinese with English abstract)
Jahn BM, Natalin’s B, Dobretsov N (2004) Phanerozoic
continental growth in Central Asia. J Asian Earth Sci
23: 599–603
Kruk NN, Rudnev SN, Vladimirov AG, Shokalsky SP,
Kovach VP, Serov PA, Volkova NI (2011) Early–Middle
Paleozoic granitoids in Gorny Altai, Russia: implications
for continental crust history and magma sources. J Asian
Earth Sci 42: 928–948
Laurent-Charvet S, Charvet J, Shu LS, Ma RS, Lu HF(2002) Paleozoic late collisional strike-slip deformations
in Tianshan and Altai, eastern Xinjiang, NW China. Terra
Nova 14: 249–256
Laurent-Charvet S, Charvet J, Monie P, Shu LS (2003)
Late Paleozoic strike-slip shear zones in eastern central
Asia (NW China): new structural and geochronological
data. Tectonics 22: doi 10.1029/2001TC901047.
Li HQ, Xie CF, Chang HL, Cai H, Zhu JP, Zhou S (1998)
Study on Metallogenetic Chronology of Nonferrous
and Precious Metallic Ore Deposits in North Xinjiang,
China. Geological Publishing House, Beijing, pp 1–264(in Chinese)
Li XR, Liu F, Yang FQ (2012) Geological times and its significance of the two mica syenogranite in the Keyinblak
Cu–Zn deposit area in Altay, Xinjiang. Xinjiang Geo 30:
5–11 (in Chinese with English abstract)
Liu F, Yang FQ, Li YH, Guo ZL, Chai FM, Geng XX,
Zhang ZX (2010) The chronology and geochemistry of
the granite from the Serbulak iron deposit in the southern
margin of Altay, Xinjiang. Acta Geol Sin 84: 195–205(in Chinese with English abstract)
Liu YL, Zhu YF, Wang DH (2003) Shear-zone related gold
deposits of the southern Altai Mountains, northwestern
China. In: Mao JW, Goldfarb RJ, Seltmann R, Wang
DH, Xiao WJ, Hart C (eds) Tectonic Evolution and
Metallogeny of the Chinese Altai and Tianshan Proceeding Volume of the International Symposium of the
IGCP-473 Project in Urumqi, pp 201–208
Liu W (1993) Whole rock isochron ages of plutons, crustal
movement and evolution of tectonics setting in the Altai Mts., Xinjiang Uygur Autonomous Region. Geosci
Xinjiang 4: 35–50 (in Chinese)Long LL, Wang YW, Wang JB, Wang LJ, Li QL, Wang
SL, Pu KX, Zhang HQ, Liao Z (2010) Magma mixing
in the Xilekuduke Cu–Mo ore district in Xinjiang: evidence from zircon U–Pb chronology. Acta Petrol Sin 26:
449–456 (in Chinese with English abstract)Tectonic and metallogenic evolution of the Chinese Altai and East Junggar

Long XP, Sun M, Yuan C, Xiao WJ, Cai KD (2008) Early
Paleozoic sedimentary record of the Chinese Altai: implications for its tectonic evolution. Sedim Geol 208: 88–100
Mao JW, Franco P, Zhang ZH, Chai FM, Wu H, Chen
SP, Cheng SL, Yang JM, Zhang CQ (2008) A reviewof the Cu–Ni sulphide deposits in the Chinese Tianshan
and Altai orogens (Xinjiang Autonomous Region, NW
China): principal characteristics and ore-forming processes. J Asian Earth Sci 32: 184–203
Mei HJ, Yang XC, Wang JD, Yu XY, Liu TG, Bai ZH(1993) The trace element geochemistry of Late Paleozoic
volcanic rocks on the southern side of Ertix River andthe evolutional history of tectonic setting. In: Tu GZ (ed)New Improvement of Gold Geosciences in Northern
Xinjiang. Beijing Science Publishing House, Beijing,
pp 199–216 (in Chinese)
Niu HC, Xu JF, Yu XY, Chen FR, Zheng ZP (1999) Discovery of Mg-rich volcanic rock series in the western Altai
area, Xinjiang, and its geologic significance. China Sci
Bull 44: 1685–1687
Niu HC, Sato H, Zhang H, Ito J, Yu Z, Nagao T, Terada
K, Zhang Q (2006) Juxtaposition of adakite, boninite,high-TiO2 and low-TiO2 basalts in the Devonian southern
Altai, Xinjian, NW China. J Asian Earth Sci 28: 439–456
Qu GS, Zhang JL (1991) Irtys structural zone. Geosci
Xinjiang 3: 115–131 (in Chinese with English abstract)
Rui ZY, Goldfarb RJ, Qiu YM, Zhou TH, Pirajno F, Yun
G (2002) Paleozoic–early Mesozoic gold deposits of
the Xinjiang Autonomous Region, Northwestern China.
Miner Depos 37: 393–418
Safonova I, Seltmann, R, Kröner A, Gladkochub D, Schulmann K, Xiao W, Kim T, Komiya T, Sun M (2011) A newconcept of continental construction in the Central Asian
Orogenic Belt (compared to actualistic examples fromthe Western Pacific). Episodes 34: 186–194
Şengör AMC, Natal’in BA, Burtman VS (1993) Evolutionof the Altaids collage and Paleozoic crustal growth inEurasia. Nature 364: 299–307
Şengör AMC, Natal’in BA, Burtman V S (1996) Turkictype orogeny and its role in the making of the continental
crust. Ann Rev Earth Planet Sci 24: 263–337
Sun M, Yuan C, Xiao WJ, Long XP, Xia XP, Zhao GC,
Lin SF, Wu FY, Kröner A (2008) Zircon U–Pb and Hf
isotopic study of gneissic rocks from the Chinese Altai:
progressive accretionary history in the early to middle
Palaeozoic. Chem Geol 247: 352–383
Thorkelson DJ, Breitsprecher K (2005) Partial melting
of slab window margins: genesis of adakitic and nonadakitic magmas. Lithos 79: 25–41
Travin AV, Boven A, Plotnikov AV, Vladimirov VG,
Theunissen V, Ladimirov AG, Melnikov AI, Titov AV(2001) 40Ar/39Ar dating of ductile deformations in the
Irtysh shear zone eastern Kazakhstan. Geochem Int 39:
1237–1241

Wan B, Zhang LC, Xiang P (2010) The Ashele VMS-type
Cu–Zn deposit in Xinjiang, NW China formed in a rifted
arc setting. Resour Geol 60:150–164
Wan B, Xiao WJ, Han CM, Brian FW, Zhang LC, Qu WJ,
Du AD (2014) Re–Os molybdenite age of the Cu–Mo
skarn ore deposit at Suoerkuduke in East Junggar, NW
China and its geological significance. Ore Geol Rev 56:
541–548
Wang DH (2003) Geology, geochemistry and geodynamics
of the Ashele VHMS Cu–Zn deposit, northwestern Xinjiang. In: Mao JW, Goldfarb RJ, Seltmann R, Wang DH,
Xiao WJ, Hart C (eds) Tectonic Evolution and Metallogeny of the Chinese Altai and Tianshan. Proceeding
Volume of the International Symposium of the IGCP-473
Project in Urumqi, pp 153–168
W ang DH, C hen YC, X u ZG, L i TD, F u XJ (2002)
Minerogenetic series of mineral deposits and regularityof mineralization in the Altaid metallogenic province,
Xinjiang, China. Atomic Energy Press, Beijing, pp 1–498(in Chinese)
Wang JB, Qin KZ, Wu ZL, Hu JH, Deng JN (1998) Volcanic–Exhalative–Sedimentary Lead–Zinc Deposits at
the Southern Margin of the Altai, Xinjiang. Geological
Publishing House, Beijing, pp 1–210 (in Chinese)
Wang JB, Wang YW, Wang S L, Ding RF (2003) The
Koktal Pb–Zn massive sulfide deposit. In: Mao JW,
Goldfarb RJ, Seltmann R, Wang DH, Xiao WJ, Hart
C (eds) Tectonic Evolution and Metallogeny of theChinese Altai and Tianshan. Proceeding Volume of theInternational Symposium of the IGCP-473 Project in
Urumqi, pp 169–180
Wang RM, Zhao CL, Ma WP, Zhou YX, Zhang YB (1991)
No. 1 Ore Deposit at Kalatongke of Xinjiang. Geological
Publishing House, Beijing, pp 1–319 (in Chinese)
Wang T, Hong DW, Tong Y, Han BF, Shi YR (2005)
Zircon U–Pb SHRIMP age and origin of post-orogenic
Lamazhou granitic pluton form Altai orogen: its implications for vertical continental growth. Acta Petrol Sin 21:
640–650 (in Chinese with English abstract)
Wang YW, Wang JB, Wang SL, Ding RF, Wang LJ (2003)
Geology of the Mengku iron deposit, Xinjiang, China– a metamorphosed VMS? In: Mao JW, Goldfarb RJ,
Seltmann R, Wang DH, Xiao WJ, Hart C (eds) Tectonic
Evolution and Metallogeny of the Chinese Altai andTianshan. Proceeding Volume of the International Symposium of the IGCP-473 Project in Urumqi, pp 181–200
Wang YW, Wang JB, Wang SL, Long LL, Wang LJ, Pu
KX, Wang SD, Tang PZ (2010) Geological characteristics and genesis of the Xilekuduke Cu–Mo deposit,
Xinjiang. Xinjiang Geol 28: 370–376 (in Chinese withEnglish abstract)
Wang Z (1991) Geological feature of Duolanasayi gold
deposit in Xinjiang. Xinjiang Geol 9: 72–79 (in Chinesewith English abstract)273

Chunming Han, Wenjiao Xiao, Guochun Zhao, Benxun Su, Patrick Asamoah Sakyi, Songjian Ao, Bo Wan, Jien Zhang, Zhiyong Zhang, Zhongmei Wang

Windley BF, Kröner A, Gu JH, Qu GS, Li YY, Zhang C(2002) Neoproterozoic to Paleozoic geology of the Altai
orogen, NW China: new zircon age data and tectonic
evolution. J Geol 110: 719–739
Windley BF, Alexeiev D, Xiao W J, Kröner A, Badarch
G (2007) Tectonic models for accretion of the Central
Asian Orogenic Belt. J Geol Soc, London 164: 31–47
Wu GG, Dong LH, Xue CJ, Feng J, Tan HD, Zhang ZC,
Wen CS, Zhou G, Gong QJ, Gao JG, Du YS, He MY,
Liu JL, Tu QJ (2008) The Main Porphyry Copper Ore
Belts in Northern Xinjiang China. Geological Publishing
House, Beijing, China, pp 1–345 (in Chinese)
Xiao WJ, Windley BF, Badarch G, Sun S, Li JL, Qin KZ,
Wang ZH (2004) Palaeozoic accretionary and convergent
tectonics of the southern Altaids: implications for the lateral
growth of Central Asia. J Geol Soc, London 161: 339–342
Xiao WJ, Han CM, Yuan C, Sun M, Lin SF, Chen HL, Li
ZL, Li JL, Sun S (2008) Middle Cambrian to Permian
subduction-related accretionary orogenesis of Northern
Xinjiang, NW China: implications for the tectonic evolution of central Asia. J Asian Earth Sci 32: 102–117
Xu LG, Mao JW, Yang FQ, Daniel H, Zheng JM (2010) Geology, geochemistry and age constraints on the Mengku
skarn iron deposit in Xinjiang Altai, NW China. J Asian
Earth Sci 39: 423–440
Yan SH, Zhang ZC, Wang DH, Chen BL, He LX, Zhou G(2003) Kalatongke metallogenic copper–nickel sulfide
deposit. In: Mao JW, Goldfarb RJ, Seltmann R, Wang
DH, Xiao WJ, Hart C (eds) Tectonic Evolution and
Metallogeny of the Chinese Altai and Tianshan. Proceeding Volume of the International Symposium of the
IGCP-473 Project in Urumqi, pp 17–30
Yan SH, Chen W, Wang YT, Zhang ZC, Chen BL (2004)40
Ar/39Ar dating and its significance of the Ertix gold
metallogenic belt in the Altai orogen, Xinjiang. Acta
Geol Sinica 78: 500–505 (in Chinese)
Yang FQ, Yan SH, Qu W, Zhou G, Liu F, Geng XX, Liu
GR, Wang X (2010) The fluid inclusions and C, H andO isotopic geochemistry of the I mineralized zone at theHalasu copper deposit, Xinjiang. Earth Sci Frontier 17:
359–374 (in Chinese with English abstract)
Yang FQ, Mao JW, Pirajno F, Yan SH, Liu GR, Zhou G,
Zhang ZX, Liu F, Geng XX, Guo CL (2012) A review ofthe geological characteristics and geodynamic setting of
Late Paleozoic porphyry copper deposits in the Junggar
region, Xinjiang Uygur Autonomous Region, northwest
China. J Asian Earth Sci 49: 80–98
Yang FQ, Mao JW, Liu F, Chai FM, Geng XX, Zhang ZX,
Guo XJ, Liu GR (2013) A review of the geological characteristics and mineralization history of iron deposits in
the Altay orogenic belt of the Xinjiang, northwest China.
Ore Geol Rev 54:1–16
Yang FQ, Chai FM, Zhang ZX, Geng XX (2014) Zircon
U–Pb geochronology, geochemistry, and Sr–Nd–Hf274

isotopes of granitoids in the Yulekenhalasu copper ore
district, northern Junggar, China: petrogenesis and tectonic implications. Lithos 190–191: 85–103
Yang WP, Zhang ZC, Zhou G, Yan SH, He LX, Chen BL(2005) Discovery of the Xileketehalasu porphyry copper deposit on the southern margin of the Altai copper
metallogenic belt. Geol China 32: 107–114 (in Chinesewith English abstract)
Yakubchuk A, Seltmann R, Shatov V (2003) Tectonics
and metallogeny of the western part of the Altaid orogenic collage. In: Mao JW, Goldfarb RJ, Seltmann R,
Wang DH, Xiao WJ, Hart C (eds) Tectonic Evolution
and Metallogeny of the Chinese Altai and Tianshan.
Proceeding Volume of the International Symposium of
the IGCP-473 Project in Urumqi, pp 7–16
Yu XY, Mei HJ, Yang XC, Wang JD (1993) Ertix volcanic
rocks and tectonic evolution. In: Tu GZ (ed) NewImprovement of Gold Geosciences in Northern Xinjiang. Beijing
Science Publishing House, Beijing, pp 185–198 (in Chinese)
Zhang ZC, Mao JW, Zhou G, Chai FM, Yan SH, Chen BL(2005) Geochemistry of the Kalatongke layered intrusion, Xinjiang NW China: implications for the genesisof a magmatic Cu–Ni sulfide deposit. In: Mao JW, FrankPB (eds) Mineral Deposit Research: Meeting the Global
Challenge. Proceedings of the Eighth Biennial SGA
Meeting, Beijing, China, pp 489–502
Zhang ZC, Yan SH, Chen BL, Zhou G, He YK, Chai FM,
He LX, Wan YS (2006) SHRIMP zircon U–Pb dating
for subduction-related granitic rocks in the northern partof east Junggar, Xinjiang. Chin Sci Bull 51: 952–962
Zhang ZX, Yang FQ, Li C, Liu F, Geng XX, Liu GR, Chai
FM, Ouyang LJ (2012) Rock-forming and ore-forming
ages of Qiaoxiahala Fe–Cu–Au deposit on northern
margin of Junggar Basin, Xinjiang. Miner Depos 31:
347–358 (in Chinese with English abstract)
Zhao ZF, Xun CJ, Zhang LW, Wen CS, Zhou G, Liu GR(2009) U–Pb dating of zircons from acid intrusions in
Yulekenhalasu copper deposit of Qinghe, Xinjiang, andits geological significance. Miner Depos 28: 425–433 (inChinese with English abstract)
Zhao ZH, Wang ZG, Zou TR, Masuda A (1993) The REE,
isotopic composition of O, Pb, Sr and Nd and diagenetic
model of granitoids in Altai region. In: Tu GZ (ed) New
Improvement of Gold Geosciences in Northern Xinjiang.
Beijing Science Publishing House, Beijing, pp 1–266(in Chinese)
Zheng CQ, Kato T, Enami M, Xu XC (2007) CHIME
monazite ages of metasediments from the Altai orogenin northwestern China: Devonian and Permian ages ofmetamorphism and their significance. The Island Arc
16: 598–604
Zhou TF, Yuan F, Yue SC, Yuan XY (2000) Magmatism
and mineralization of Nuoerte in Xinjiang. Geological
Publishing House, Beijing, pp 1–125 (in Chinese)