Incremental growth and origin of the Cretaceous Renjiayingzi pluton, southern Inner Mongolia, China:...

Journal of Asian Earth Sciences 75 (2013) 226–242

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Journal of Asian Earth Sciences

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Incremental growth and origin of the Cretaceous Renjiayingzi pluton,southern Inner Mongolia, China: Evidence from structure, geochemistryand geochronology

1367-9120/$ - see front matter � 2013 Elsevier Ltd. All rights reserved.http://dx.doi.org/10.1016/j.jseaes.2013.07.005

⇑ Corresponding author. Address: Institute of Geology, Chinese Academy ofGeological Sciences, 26 Baiwanzhuang Road, Beijing 100037, China. Tel.: +86 1068999685; fax: +86 10 68999662.

E-mail address: [email protected] (S. Li).

Shan Li a,b,⇑, Simon A. Wilde b, Tao Wang a, Qianqian Guo c

a Institute of Geology, Chinese Academy of Geological Sciences, Beijing 100037, Chinab Department of Applied Geology, Curtin University, G.P.O. Box U1987, Perth, Western Australia 6845, Australiac Key Laboratory of Computational Geodynamics, University of Chinese Academy of Sciences, Beijing 100049, China

a r t i c l e i n f o

Article history:Received 7 January 2013Received in revised form 1 July 2013Accepted 3 July 2013Available online 18 July 2013

Keywords:Cretaceous plutonMagmatic emplacementIncremental growthZircon U–Pb agesZircon Hf isotopesSouthern CAOB

a b s t r a c t

The Renjiayingzi intermediate-acid pluton is located along a pre-existing ENE–WSW-trending dextralshear zone that forms part of the Xar Moron suture zone that marks the final closure of the Paleo-AsianOcean. The pluton is composed of three small intrusions, which from northwest to southeast, are namedthe Shuangjianshan (SI), the Qianweiliansu (QI) and the Xingshuwabeishan (XI) intrusions. LA-ICPMS zir-con U–Pb dating of a pyroxene diorite from the SI yields an age of 138 ± 1 Ma; the SHRIMP zircon U–Pbage of a tonalite from the QI records an age of 134 ± 2 Ma, whereas LA-ICPMS zircon U–Pb dating of amonzogranite from the XI has an age of 126 ± 1 Ma, suggesting the entire pluton was built up by threeseparate emplacement events that young to the ESE: this is further supported by the contact relations.Incremental growth of plutons by amalgamation of repeated small magma pulses is the most viableemplacement model. The pluton was probably emplaced by updoming of the roof along previous tensilefractures and by upward stacking of the three intrusions. The SI and QI have similar U–Pb ages and geo-chemical characteristics, and most likely had the same magma source and underwent similar petroge-netic processes. They have high MgO concentrations at low silica contents, are enriched in large ionlithophile elements, depleted in high field strength elements, have negative eNd(t) values of �1.8 to�3.7, with Nd model ages of 1.07–1.19 Ga. Pyroxene diorites of the SI also have variable zircon eHf(t) val-ues (from �0.8 to +6.1), indicating that they were mainly derived from juvenile crust with minor crustalcontamination and clinopyroxene-dominated fractional crystallization. The late monzogranites from theXI show weak negative eNd(t) values of �2.3 to �2.5, young Nd model ages of 0.99–1.00 Ga, positive zir-con eHf(t) values (+1.3 to +4.6) and higher SiO2 and K2O contents, with strong depletion in Eu, P and Ti,indicating derivation from a distinct petrogenetic process from the two earlier intrusions. The monzog-ranites were the result of partial melting of juvenile crust in response to mantle-derived magma under-plating, together with plagioclase-dominated fractional crystallization.

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1. Introduction

Granitic plutons play a fundamental role in the growth and dif-ferentiation of the continental crust but there is still significantcontroversy about the generation and intrusion of granitic magmasinto the crust. An increasing amount of evidence from geological,geophysical, geochemical and geochronological data (e.g.Vigneresse and Bouchez, 1997; Wang et al., 2000; Coleman et al.,2004; Michel et al., 2008; Miller, 2008; de Saint Blanquat et al.,2011; Paterson et al., 2011), as well as theoretical models (e.g.

Kavanagh et al., 2006; Menand, 2008, 2011; Annen, 2009, 2011;Michaut and Jaupart, 2011), indicates that many igneous plutonsare the result of incremental growth by the accretion and amal-gamation of several discrete and relatively small magma pulsesand injections over variable periods of time, from hundred to mil-lions of years (Petford et al., 2000; Coleman et al., 2004; Glazneret al., 2004; Matzel et al., 2006; Lipman, 2007; Miller et al., 2007;Walker et al., 2007; Burgess and Miller, 2008; Michel et al., 2008;Horsman et al., 2009; Howard et al., 2011; Davis et al., 2012). Incre-mental growth is also thought to be mechanically more viable thanquasi-instantaneous or rapid emplacement of a single large magmabody or bulk magmatic flow, and thus it alleviates the space prob-lem associated with overall inflation (e.g., Petford et al., 2000;Bartley et al., 2008; Miller, 2008; Menand, 2011). This suggests thatthe emplacement of magma bodies is a multi-timescale process

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S. Li et al. / Journal of Asian Earth Sciences 75 (2013) 226–242 227

(e.g., Matzel et al., 2006; Walker et al., 2007; Miller, 2008; Annen,2009, 2011; de Saint Blanquat et al., 2011).

The recognition of incremental growth as an emplacementmechanism has far-reaching implications and provides a new per-spective on magmatic processes and pluton construction. Accord-ing to this model, the evolution of magma bodies is related tothe processes that control the time scale and the spatial distribu-tion of the successive pulses, depending on their emplacement rateand on their ability to amalgamate (Coleman et al., 2004; Glazneret al., 2004; Miller, 2008; Annen, 2011; Menand, 2011). Indeed, itleads to new challenges for the interpretation of these processesand how they operate in governing the emplacement and growthof plutons, both in space and time (Annen, 2011; Menand, 2011;Miller et al., 2011; Paterson et al., 2011).

The Renjiayingzi pluton, located in the southernmost part of theCentral Asian Orogenic Belt (CAOB) and the southern Great Xing’anRange, NE China (Fig. 1), is an excellent locality to test the model ofincremental pluton growth because of its good exposures and com-posite intrusions, allowing examination of the composition, tex-ture, and age of the various components in detail. Mostimportantly, intrusion of each increment of magma can easily bedistinguished on the basis of compositional and textural diversity.This study presents new zircon U–Pb ages and Hf isotopes, whole-rock Sr–Nd isotopes and major and trace element compositions forthe three intrusions that make up the Renjiayingzi pluton, and pro-poses a model of incremental pluton growth.

Fig. 1. (a) Simplified geological sketch map of the Central Asian Orogenic Belt (CAOB) shKröner et al. (2008)). The location of Fig. 1b is indicated. (b) Simplified tectonic map ofFig. 2 (modified after Xiao et al. (2003) and Jian et al. (2008, 2010)). Light gray zone repr2008, 2010) or northern accretionary zone of Xiao et al. (2003), whereas the dark gray zsouthern accretionary zone of Xiao et al. (2003). Published zircon U–Pb ages for Permianet al. (2009), Liu et al. (2009, 2012), Jian et al. (2010), Zhang et al. (2010) and Wu et al.

2. Geological setting

The CAOB, or Altaids, is a complex collage of microcontinentalblocks, island arcs, and remnants of oceanic crust between theSiberia Craton to the north and Tarim and North China cratons tothe south, and is one of the largest and most complex Phanerozoicaccretionary orogenic belts, with considerable juvenile crustalgrowth (S�engör et al., 1993; Jahn et al., 2000, 2004; Windleyet al., 2002, 2007; Kovalenko et al., 2004; Kröner et al., 2008,2013; Long et al., 2012; Xiao et al., 2009a, 2013). Inner Mongoliais situated in the southernmost part of the CAOB along the Solon-ker suture zone, between the Tianshan Orogenic Belt to the westand the Songliao Basin to the east (Fig. 1b). This segment wasmainly constructed by convergent processes between the activemargin of the South Mongolia terranes (or South Mongolia-GobiBlock) to the north and the northern margin of the North ChinaCraton to the south and recorded the final closure of the Paleo-Asian Ocean and termination of collisional activity in the CAOB(Xiao et al., 2003, 2009b; Kovalenko et al., 2004; Li, 2006; Jianet al., 2010; Windley et al., 2010) (Fig. 1a).

The study area is situated in southern Inner Mongolia and con-sists, from north to south, of the northern continental block, theSolonker suture zone and the southern continental block (Xiaoet al., 2003; Jian et al., 2008, 2010) (Fig. 1b). The northern continen-tal block consists of the Late Carboniferous (ca. 310, Chen et al.,2000, 2009) Baolidao arc and associated Precambrian blocks (e.g.,

owing the main tectonic sub-divisions (modified after Jahn et al. (2000, 2004) andthe southeastern CAOB showing the main tectonic subdivisions and the location ofesents the northern Early-Mid Paleozoic orogen and the Hutag Uul Block (Jian et al.,one represents the southern Early-Mid Paleozoic orogen (Jian et al., 2008, 2010) or

–Triassic magmatic rocks in the region are shown and are from Li et al. (2007), Chen(2011).

228 S. Li et al. / Journal of Asian Earth Sciences 75 (2013) 226–242

Xilin Gol metamorphic complex) (Xiao et al., 2003; Chen et al.,2009; Li et al., 2011; Xu et al., 2012). The southern continentalblock between the North China Craton and the Solonker suturezone is characterized by Early Ordovician to Early Silurian (ca.488–438 Ma) subduction–accretion complexes and arc-relatedigneous rocks (Jian et al., 2008; Xu et al., 2012; Zhang et al.,2012). The final subduction of the Paleo-Asian Ocean caused thetwo opposing continental margins to collide (Xiao et al., 2003;Chen et al., 2009), leading to formation of the Solonker suture zonein the Permian (Li, 2006; Chen et al., 2009; Li et al., 2009; Jian et al.,2010). The Solonker suture zone is marked by the Solonker–XarMoron ophiolitic belt (Li, 2006; Li et al., 2009; Jian et al., 2010;Zhou and Wilde, 2012) (Fig. 1b). This suture recorded the terminalevents in the southern CAOB in Inner Mongolia, and there followeda sequence of tectono-magmatic events during the Middle-LatePermian in response to block convergence and resulted in Triassicpost-collisional/orogenic extension in the area (Xiao et al., 2003; Li,2006; Jian et al., 2010; Windley et al., 2010).

The crust was uplifted in the Early Jurassic, as evidenced by theabsence of the Early Jurassic sediments (BGMRIM, 1991, 1996).During the late Middle through early Late Jurassic time, collisionof the combined North China–Mongolia block along the Mongol–Okhotsk belt to the north resulted in NE–SW thrust faulting, crus-tal thickening and inversion structures in the various Mesozoic ba-sins that had developed in the area (Zorin, 1999; Badarch et al.,2002; Kravchinsky et al., 2002; Meng, 2003; Wang et al., 2011).The extensional events include rift basins, alkaline and peralkalinegranitoid plutonism, as well as metamorphic core complexes in

Fig. 2. Distribution map of granitoids in the Linxi area of southern Inner Mongolia, Chlocation of the Renjiayingzhi pluton (modified after BGMRIM (1995, 1996)). Published zirLiu et al. (2009, 2012), Zhang et al. (2010), Wu et al. (2011) and Jiang et al. (2012).

northern Inner Mongolia in the latest Late Jurassic to the Early Cre-taceous, related to extensional collapse after the collision of theMongol–Okhotsk belt and this was further influenced by west-directed circum-Pacific subduction (Webb et al., 1999; Daviset al., 2009; Jahn et al., 2009; Zhou et al., 2009; Lin et al., 2011;Wang et al., 2011). Rift basins were initiated by voluminous volca-nic eruption, and culminated in the Early Cretaceous (Meng, 2003).These extensional basins underwent little or no post-rift thermalsubsidence, which, when integrated with intense granitoid pluto-nism, implies an elevated geothermal gradient in the Early Creta-ceous (Bialas et al., 2010).

Volcanism and granitoid plutonism occurred widely in the areafrom the Late Paleozoic through to the Late Mesozoic. Many gran-itoid intrusions were emplaced in the Permian, Triassic, Late Juras-sic, and particularly the Early Cretaceous (Liu et al., 2005, 2009;Wu et al., 2011; Fig. 2). The Renjiayingzi pluton is located to thenorth of the Xar Moron River, where Silurian slate, Permian clasticrocks and Cretaceous volcanic rocks are exposed (BGMRIM, 1991,1996) (Fig. 1b and Fig. 2).

3. Renjiayingzi pluton and structural patterns

The Renjiayingzi pluton is located about 35 km southeast of Lin-xi (Fig. 2) and has an irregular oval shape with an area of ca.4.5 km2 (Fig. 3). It intruded into Permian sandstone and sandy con-glomerate, and itself was intruded by Cretaceous subvolcanic rocksin the west. The pluton has a 1 km-wide metamorphic (hornfelsed)

ina, showing the predominately NE-trending Early Cretaceous granitoids and thecon U–Pb ages for granitoids in the region are from Li et al. (2007), Chen et al. (2009),

Fig. 3. Geological map of the Renjiayingzhi pluton and surrounding rocks in southern Inner Mongolia (modified after BGMRIM (1995)).


aureole along the contacts with sandstone and sandy conglomerate(Fig. 3). The most striking structural features in this area are bed-ding-oblique ductile shear zones, which developed in the Permianclastic rocks (BGMRIM, 1995, 1996; Wang et al., 1999; Fig. 3). Theregional foliation of the wall rock strikes 060–130� and the stretch-ing lineation plunges to the ENE from sub-horizontal to �15�(BGMRIM, 1995, 1996; Wang et al., 1999). The pluton is composed,from NW to SE, of three semi-circular intrusions or units: the Shu-angjianshan Intrusion (SI), the Qianweiliansu Intrusion (QI) and theXingshuwabeishan Intrusion (XI) (Fig. 3).

Field observations indicate that the oldest magmatic unit is theShuangjianshan Intrusion (SI), composed of fine- to medium-grained pyroxene diorite with minor hornblende diorite, with itsnorthwestern margin overlain by Cretaceous volcanic rocks. Theunit has an area of �1.4 km2 and is semi-circular in shape(Fig. 3). It intruded Permian clastic rocks in the south, and the con-tacts dip 50–80�. Magmatic foliations are present, characterized byalignment of plagioclase and pyroxene parallel to the boundary ofthe intrusion, and these dip inward at 35–65�. The pyroxene dioriteconsists of plagioclase (70–80%), clinopyroxene (20–30%), quartz(1%) and hornblende (1%) (Fig. 4a). Accessory minerals are zircon,magnetite, apatite, ilmenite and titanite.

Fig. 4. Photomicrographs of the Renjiayingzi pluton. (a) Pyroxene diorite (11RJ-2) from tQt: Quartz, Kf: K-feldspar, Pl: Plagioclase, Bt: Biotite, Hb: Hornblende and Cpx: Clinopyr

The next unit to the ESE is the Qianweiliansu Intrusion (QI),composed of fine- to medium-grained tonalite with minor quartzdiorite. Contact relationships with the SI are locally complex andappear transitional. The QI has an area of �1.5 km2, and is alsosemi-circular in shape (Fig. 3). It intruded into Permian clasticrocks, with outward dips of 35–50�. Magmatic foliations are pres-ent and characterized by alignment of plagioclase, hornblende and/or pyroxene, parallel to the margins of the intrusion. The foliationsdip either outward or inward at 20–45�. The tonalite consists ofplagioclase (60–70%), K-feldspar (1–5%), quartz (5–15%), biotite(2–8%), hornblende (1–5%) and clinopyroxene (1–5%) (Fig. 4b).Accessory minerals are zircon, magnetite, apatite, ilmenite andtitanite.

The youngest magma pulse is the Xingshuwabeishan Intrusion(XI), mainly composed of monzogranite with minor quartz monzo-nite and containing same diorite xenoliths. It is exposed over anarea of �1.6 km2 and is oval shaped (Fig. 3). It intruded into theQI and Permian clastic rocks, with outward-dipping contacts of35–60�. In general, magmatic foliations are less well-defined in thisunit, and are characterized by weak alignment of biotite, K-feld-spar or plagioclase, parallel to the margins of the intrusion; theydip outward at angles of �35�. The monzogranite is composed of

he SI, (b) Tonalite (11RJ-5) from the QI and (c) Monzogranite (11RJ-11) from the XI.oxene.

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plagioclase (30–40%), K-feldspar (30–40%), quartz (20–30%), biotite(2–8%) and hornblende (1–5%) (Fig. 4c). Accessory minerals are zir-con, magnetite, apatite, ilmenite and titanite.

4. Zircon U–Pb dating for the three intrusions

The LA-ICPMS (samples 11RJ-2 and 11RJ-11) and SHRIMP (sam-ple 11RJ-5) zircon U–Pb analyses are listed in Tables 1a and 1b,respectively. Zircon grains from pyroxene diorite (sample 11RJ-2)of the SI range in size from 50 to 150 lm and have length to widthratios between 1:1 and 3:1, and are mostly colorless, transparentand predominantly euhedral tabular crystals. In CL images(Fig. 5a), they commonly exhibit weak oscillatory zoning, indica-tive of magmatic crystallization. Most have moderate to high Uand Th concentrations (av. 700 and 919 ppm, respectively) andhigh Th/U ratios (0.5–2.1). Twenty-seven spots were analyzedand 25 of them yield 206Pb/238U ages ranging from 130 to142 Ma. The most concordant 20 points define a weighted mean206Pb/238U age of 138 ± 1 Ma with an MSWD = 1.7 (Fig. 6a), inter-preted as the formation age of the pyroxene diorite. In addition,two analyses are older with 206Pb/238U ages of 167 ± 2 Ma and231 ± 3 Ma, suggesting they are inherited zircons.

Zircon grains from tonalite (sample 11RJ-5) of the QI range insize from 100 to 300 lm and have length to width ratios between1:1 and 3:1, and are mostly colorless, transparent and euhedralstubby prismatic crystals. In CL images (Fig. 5b), they commonlyexhibit magmatic oscillatory zoning. Most have high U and Th con-centrations (av. 1189 and 1251 ppm, respectively) and high Th/Uratios (0.5–1.4). Eleven sites were analyzed and yield 206Pb/238Uages ranging from 131 to 140 Ma. Most data are concordant anddefine a weighted mean 206Pb/238U age of 134 ± 2 Ma with anMSWD = 1.4 (Fig. 6b), interpreted as the formation age of thetonalite.

Fig. 5. Cathodoluminescence (CL) images of selected zircon grains from (a) Pyroxene d(11RJ-11) from the XI. The locations of U–Pb spot analyses are shown as small circles, whfor U–Pb sites refer to spot numbers in Table 1.

Fig. 6. U–Pb concordia diagrams showing zircon ages obtained by LA-ICPMS and SHRIMthe QI by SHRIMP and (c) Monzogranite (11RJ-11) from the XI by LA-ICPMS.

Zircon grains from monzogranite (sample 11RJ-11) of the XIrange in size from 30 to 150 lm and have length to width ratiosbetween 1:1 and 3:1, and are mostly clear and transparent. Mostgrains are subhedral and in CL images (Fig. 5c) they show weakbanding, indicative of magmatic crystallization. Most have low Uand Th concentrations (av. 217 and 204 ppm, respectively) andhigh Th/U ratios (0.7–1.2). Twenty-eight sites were analyzed andall are concordant. The 12 youngest analyses yield 206Pb/238U agesranging from 124 to 129 Ma, defining a weighted mean 206Pb/238Uage of 126 ± 1 Ma with an MSWD = 0.4 (Fig. 6c), and this is inter-preted as the formation age of the monzogranite. In addition, 15spots show 206Pb/238U ages of 130–142 Ma, suggesting they areinherited zircons probably from the older SI and the QI; one sub-rounded zircon has a 206Pb/238U age of 241 ± 1 Ma, indicating it isinherited zircon from an older source.

5. Whole-rock geochemistry, Sr–Nd isotopes and zircon Hfisotopes

5.1. Major and trace element geochemistry

The major and trace element data are presented in Table 2. TheSI and the QI have high contents in TFe2O3 (6.36–7.55%), MgO(2.32–4.68%) and CaO (4.84–6.97%), and moderate contents inNa2O (3.93–4.27%) and K2O (1.62–2.80%). They mostly plot in thehigh-K calc-alkaline field (Fig. 7a) and their A/CNK ratios rangefrom 0.82 to 0.89, indicating that they are metaluminous(Fig. 7b). They plot within or adjacent to the calc-alkalic field(Fig. 7c) and straddle the ferroan to magnesian fields of A-typegranitoids (Fig. 7d) in the classification diagrams of Frost et al.(2001).

The XI samples have high contents in Na2O (4.42–4.54%) andK2O (4.24–4.66%), and low contents in TFe2O3 (3.13–3.49%), MgO

iorite (11RJ-2) from the SI, (b) Tonalite (11RJ-5) from the QI and (c) Monzograniteereas sites of in situ Lu–Hf isotopic analyses are shown as large circles. The numbers

P. (a) Pyroxene diorite (11RJ-2) from the SI by LA-ICPMS, (b) Tonalite (11RJ-5) from

Table 2Chemical compositions of rocks from the Renjiayingzi pluton in southern Inner Mongolia, China.

Intrusion Shuangjianshan intrusion (SI) Qianweiliangshu intrusion (QI) Xingshuwabeishan intrusion (XI)

Sample 11RJ-1 11RJ-2 11RJ-3 11RJ-5 11RJ-6 11RJ-7 11RJ-10 11RJ-11 11RJ-12 11RJ-13

Major elements (wt.%)SiO2 59.20 56.35 59.58 59.92 55.28 59.74 58.97 67.61 67.87 68.52TiO2 1.00 1.08 1.01 1.05 1.36 1.26 1.12 0.54 0.49 0.50Al2O3 16.82 16.97 16.45 16.42 17.62 17.09 16.81 14.54 14.62 14.50Fe2O3 1.93 1.83 3.34 1.91 2.61 2.25 2.35 1.99 2.01 2.07FeO 4.35 5.15 2.85 4.00 4.65 3.75 3.90 1.35 1.10 0.95MnO 0.10 0.11 0.10 0.09 0.10 0.09 0.09 0.11 0.09 0.07MgO 3.24 4.68 3.15 3.21 2.94 2.32 3.25 1.39 1.30 1.31CaO 5.86 6.67 4.84 5.35 6.97 5.25 5.47 1.74 1.79 2.16Na2O 4.08 4.10 4.27 4.00 4.04 4.22 3.93 4.42 4.54 4.45K2O 2.29 1.75 2.48 2.57 1.62 2.80 2.25 4.48 4.66 4.24P2O5 0.26 0.27 0.28 0.26 0.41 0.38 0.31 0.13 0.12 0.13

LOI 0.35 0.47 1.21 0.66 1.73 0.35 0.97 1.41 1.13 0.85

Total 99.48 99.43 99.56 99.45 99.33 99.50 99.42 99.71 99.72 99.76

Tarce elements (ppm)La 24.4 20.6 23.3 28.6 28.3 31.3 24.4 27.5 29.5 35.3Ce 50.3 42.2 35.7 58.0 58.6 63.9 53.0 59.8 53.8 69.3Pr 6.4 5.6 6.0 7.2 7.4 8.2 6.6 6.4 6.6 7.7Nd 26.90 23.20 26.30 30.00 33.20 32.30 28.00 25.40 25.10 28.00Sm 5.15 4.33 5.38 5.43 6.30 7.06 4.94 4.32 4.64 4.58Eu 1.56 1.31 1.46 1.49 1.63 1.78 1.47 0.99 0.78 0.99Gd 4.42 3.62 4.51 4.44 5.86 5.27 4.00 3.37 3.15 3.72Tb 0.75 0.67 0.81 0.78 1.06 0.98 0.71 0.59 0.65 0.67Dy 4.42 3.47 4.68 4.45 5.75 4.94 3.19 3.52 3.12 3.39Ho 0.74 0.60 0.75 0.75 1.12 0.88 0.64 0.64 0.55 0.66Er 2.35 1.82 2.39 2.09 3.34 2.63 1.87 1.70 1.59 1.93Tm 0.35 0.26 0.34 0.29 0.50 0.37 0.25 0.30 0.30 0.28Yb 2.44 1.96 1.93 1.91 2.97 2.46 1.58 2.03 1.71 2.05Lu 0.42 0.25 0.37 0.31 0.50 0.38 0.25 0.34 0.28 0.32Y 24.0 17.6 21.3 22.5 32.0 25.1 18.0 18.7 16.5 20.4Sc 14.3 16.4 20.7 12.2 14.1 11.5 12.7 5.9 8.0 5.4V 143 154 125 142 182 147 142 58 54 62Cr 33 88 40 57 27 31 35 21 20 19Co 19 23 14 19 21 16 20 5 7 6Ni 10 24 10 17 12 12 13 8 8 6Ga 20 19 20 21 23 21 20 18 19 18Rb 64 34 59 99 55 101 74 123 148 160Sr 744 824 631 764 853 742 887 290 296 382Zr 154 77 66 155 94 241 111 282 283 254Nb 6.5 5.0 7.6 7.5 10.3 9.0 6.9 9.5 9.5 9.4Cs 2.8 1.6 3.3 5.4 9.1 5.7 4.4 5.0 5.5 5.4Ba 765 725 857 704 486 815 759 742 814 675Hf 4.1 2.9 2.8 4.7 2.8 7.2 3.6 8.7 8.4 8.9Ta 0.53 0.40 0.65 0.77 1.18 0.86 0.54 1.31 1.31 1.31Pb 11 8 7 14 12 15 10 14 158 55Th 6 3 4 11 8 11 6 23 24 31U 1.2 0.8 0.4 3.5 4.2 3.7 1.4 3.3 2.4 3.0

RREE 130.56 109.86 113.92 145.73 156.56 162.42 130.88 136.91 131.77 158.92(La/Yb)N 7.17 7.54 8.66 10.74 6.83 9.13 11.08 9.72 12.37 12.35dEu 0.97 0.98 0.88 0.90 0.80 0.85 0.98 0.76 0.59 0.71


(1.30–1.39%) and CaO (1.74–2.16%). They plot in the high-K calc-alkaline field (Fig. 7a), and their A/CNK ratios range from 0.92 to0.95, indicating that they are metaluminous, although they plotwell away from the field of the SI and QI samples (Fig. 7b). Theystraddle the alkali-calcic to alkalic fields (Fig. 7c) and plot in themagnesian field (Fig. 7d) in the Frost et al. (2001) diagram. Thesecharacteristics are broadly similar to other Early Cretaceous grani-toids in the area (Figs. 7 and 8).

As shown on the major oxide variation diagrams (Fig. 8), mostsamples from the Renjiayingzi pluton define a magmatic evolutiontrend: TiO2, Al2O3, TFe2O3, P2O5, MgO and CaO are negatively corre-lated with SiO2, whereas K2O and Na2O are positively correlated.MnO, however, is more scattered. Note that there is a composi-tional gap in SiO2 content from 60% to 68%.

The chondrite-normalized rare earth element patterns (Fig. 9a)are fractionated and show a range of RREE from 109.9 to 162.4

with the XI showing the largest negative Eu anomalies (dEu from0.59 to 0.76). In the primitive mantle-normalized spidergram(Fig. 9b), all samples show moderate depletion in high fieldstrength elements (HFSE, such as Nb, Ta, P and Ti) and moderateenrichment in light REE (LREE, such as La, Ce and Nd). However,the SI has negative Th anomalies and positive Ba anomalies,whereas the QI shows positive anomalies for both Th and Ba; theXI records negative anomalies for Ba and positive anomalies for Th.

5.2. Sr–Nd isotopes

Whole-rock Rb–Sr and Sm–Nd isotopic compositions for sixsamples are presented in Table 3. These data are compared on aSr–Nd isotopic diagram (Fig. 10) with published compositions forEarly Cretaceous granitoids from the Xiaochengzi pluton along

Fig. 7. Selected major element diagrams for the Renjiayingzi pluton. (a) K2O vs. SiO2 diagram (after Peccerillo and Taylor (1976)), (b) A/NK vs. A/CNK diagram (after Maniarand Piccoli, 1989), (c) Na2O + K2O–CaO vs. SiO2 diagram (after Frost et al. (2001)), (d) TFeO/(TFeO + MgO) vs. SiO2 diagram (after Frost and Frost (2008)). TFeO = FeO + 0.9 Fe2O3,A/CNK = mol Al2O3/(Na2O + K2O + CaO), A/NK = mol Al2O3/(Na2O + K2O). Data for the Early Cretaceous granitoids in the Linxi area are from Liu et al. (2005).


the Xar Moron suture zone (Fig. 2) and the northern continentalblock.

The initial 87Sr/86Sr ratios (Sri) and eNd(t) values have been cal-culated on the basis of the zircon U–Pb ages for these intrusions.The Sri values of pyroxene diorites from the SI are 0.7058 and eNd(t)values vary from �1.8 to �3.2 (Fig. 10), with Nd model ages of1.07–1.18 Ga. Similarly, the Sri values of tonalites from the QI rangefrom 0.7057 to 0.7058 and eNd(t) values vary from �2.0 to �3.7(Fig. 10), with Nd model ages of 1.15–1.16 Ga. The monzogranitesfrom the XI show slightly higher Sri values (0.7060–0.7061), weaknegative eNd(t) values (�2.3 to �2.5) and slightly younger Nd mod-el ages (0.99–1.00 Ga) than those of the SI and QI, indicating less ofa crustal signature in the magma source.

5.3. Zircon Hf isotopes

In situ zircon Hf isotopic analyses from two samples are listedin Table 4 and presented in Fig. 11. They were made on the samezircons, but from different sites, used for U–Pb dating due to thelarge size of the laser ablation pits (Fig. 5). Thirteen zircon grainsfrom pyroxene diorite sample 11RJ-2 from the SI, with a weightedmean 206Pb/238U age of 138 ± 1 Ma, have variable Hf isotopic com-positions with 176Hf/177Hf ratios of 0.282681–0.282865, eHf(t)values of �0.8 to +6.1 and two-stage model ages (TDM2) of 0.80–1.24 Ga. Fifteen zircon grains from monzogranite sample 11RJ-11from the XI were also analyzed. Six of them, with a weighted mean206Pb/238U age of 126 ± 1 Ma, have uniform Hf isotopic composi-tions, with 176Hf/177Hf ratios of 0.282731–0.282825, eHf(t) values

of +1.3 to +4.6 and two-stage model ages (TDM2) of 0.89–1.10 Ga.The other nine zircons with 206Pb/238U ages of 130–142 Ma alsoshow similar Hf isotopic compositions, with 176Hf/177Hf ratios of0.282717–0.282824, eHf(t) values of +0.8 to +4.8 and two-stagemodel ages (TDM2) of 0.89–1.14 Ga. All samples show a spread frommildly negative eHf(t) values close to the chondrite line to positivevalues as high as +6.1, suggesting mixing of slightly older crustalcomponents with juvenile magma.

6. Discussion

6.1. Emplacement time of the three granitic units

On the 1:50,000 scale geological map (BGMRIM, 1995) it isshown that the Renjiayingzi pluton is shown as a Late Triassic plu-ton intruded into the Middle Permian Zhesi Formation. However,because of the lack of systematic geochronological and geochemi-cal studies, the exact emplacement age and its tectonic implica-tions are not constrained. The new LA-ICPMS and SHRIMP zirconU–Pb ages in this paper indicate that the Renjiayingzi pluton crys-tallized in the Early Cretaceous and constrain the emplacement or-der as the SI (138 ± 1 Ma), QI (134 ± 2 Ma) and XI (126 ± 1 Ma)(Fig. 6). Thus the Renjiayingzi pluton was built up of three separatemagmatic pulses, with the interval between the SI and the QI span-ning �4 Ma, and the XI separated from the QI by �8 Ma. Severalinherited zircons in the XI correlate with the ages of the two olderintrusions.

Fig. 8. Major oxide (wt.%) variation diagrams revealing a compositional gap in SiO2 from 60% to 68%. Symbols as in Fig.7.


The sequence of emplacement supports the field observationsconcerning the contact relations of the three intrusions. For exam-ple, the magmatic foliations vary from stronger to weaker from theearly SI to the late XI. The monzogranites of the XI also contain asmall number of dark dioritic enclaves. The magma also evolvedfrom pyroxene diorite, through tonalite, to monzogranite, a normalmagmatic evolutionary sequence. Geochemical compositions alsoevolve from mafic to felsic (see below).

6.2. Magma sources and origin

The contents of TFe2O3, MgO and CaO and Cr and Ni concentra-tions in the SI and QI are relatively higher than those of the XI,whereas the contents of SiO2 Na2O and K2O are lower than thoseof the XI, suggesting that their parental magma was mantle-de-rived. As shown on the major oxide variation diagrams (Fig. 8),there is a compositional gap in SiO2 from 60% to 68%, indicatingthese rocks are not wholly continuous and may have involved dif-ferent sources. The SI and the QI are similar in age and composition(Figs. 7 and 8), as reflected by the diffuse contacts between them.In addition, the monzogranites from the XI contain lower HREEthan the pyroxene diorites from the SI and tonalites from the QI(Fig. 9a). Furthermore, the monzogranites have more fractionated

REE patterns and stronger negative Eu anomalies, compared withthe two early intrusions (Fig. 9a). The SI and QI are also character-ized by higher ratios of Sr/Y, Nb/Ta and Ba/Rb. However, the pyrox-ene diorites from the early SI reveal a negative anomaly for Th andpositive anomaly for Ba, whereas the tonalites of the QI show po-sitive anomalies of both Th and Ba. In contrast, monzogranites ofthe younger XI exhibit negative anomalies for Ba and positiveanomalies for Th, which may be related to decreasing amounts ofpyroxene in the magma chamber with time (Fig. 9b). The monzog-ranites show slightly higher Sri values (0.7060–0.7061), slightlynegative eNd(t) values (�2.3 to �2.5) and younger Nd model ages(0.99–1.00 Ga) than those of the earlier SI and QI, indicating lessof a crustal signature in the magma source. The positive zirconeHf(t) values and young model ages suggest a dominantly juvenilesource for all granitoids of the Renjiayingzi pluton. The geochrono-logical, geochemical data and zircon Hf isotopes indicate that the SIand QI were likely derived from different source regions than theXI, or else were generated by different petrogenetic processes. Interms of the eNd(t) values, Sri values and zircon eHf(t) values(Figs. 10 and 11), the Renjiayingzi pluton tends to display moreunradiogenic initial isotopes than those of the northern continentalblock, suggesting that greater amounts of old continental crustalmaterials were involved in the magma source.

Fig. 9. (a) Chondrite-normalized rare earth element patterns and (b) Primitivemantle-normalized trace element spider diagram for the Renjiayingzi pluton. Thevalues of chondrite primitive mantle are from Sun and McDonough (1989).

Fig. 10. eNd(t) vs. Sri diagram for the Renjiayingzi pluton. Data for the EarlyCretaceous Xiaochengzi pluton and Proterozoic gneisses in this belt and the EarlyCretaceous granitoids in the northern continental block are from Liu et al. (2005).


The SI and QI have similar U–Pb ages, geochemical and isotopiccharacteristics, and most likely were derived from the same mag-ma source. They have weak negative eNd(t) values (�1.8 to �3.7)and zircon eHf(t) values (�0.8 to +6.1) (Figs. 10 and 11), recordingsome involvement of old crustal materials in their generation,but indicating derivation mainly from juvenile crust, with somesubsequent crustal contamination or a possible contribution froma subduction–accretion complex (pelagic sediments) (Liu et al.,2009). The pyroxene diorite sample (11RJ-2) has inherited zirconspotentially indicating wall-rock contamination. The correlationsbetween CaO, Al2O3, MgO and SiO2 in the SI and QI (Fig. 8) are con-sistent with clinopyroxene and/or plagioclase fractionation. Clino-pyroxene fractionation is also supported by the Ni and V vs. Crdiagrams (Figs. 12a and 12b). However, the absence of negative

Table 3Sr–Nd isotopic data from the Renjiayingzi pluton in southern Inner Mongolia, China.

No. Sample Intrusion Rb(ppm)

Sr(ppm)

87Rb/86Sr 87Sr/86Sr 2r S

1 11RJ-2 SI (pyroxene diorite) 34.7 855.0 0.118 0.70602 14 02 11RJ-3 SI (pyroxene diorite) 59.5 787.0 0.219 0.70625 11 03 11RJ-5 QI (tonalite) 88.6 719.0 0.357 0.70645 16 04 11RJ-6 QI (tonalite) 50.3 813.0 0.179 0.70608 14 05 11RJ-11 XI (monzogranite) 174.0 362.0 1.387 0.70855 13 06 11RJ-12 XI (monzogranite) 195.0 330.0 1.708 0.70902 11 0

Note: eNd = ((143Nd/144Nd)s/(143Nd/144Nd)CHUR � 1) � 10,000, fSm/Nd = (147Sm/144Nd)s/((147Sm/144Nd)CHUR = 0.1967. The model ages (TDM) were calculated using a linea((147Sm/144Nd)s � 0.2137)).

Sr and Eu anomalies in the primitive mantle-normalized trace ele-ment diagrams (Fig. 9b) precludes extensive plagioclase fraction-ation. The decrease in total Fe2O3 and TiO2 concentrations withdecreasing SiO2 contents (Fig. 8) may be the result of fractionalcrystallization of Fe–Ti oxides. The abundances of P2O5 decreaseswith increasing SiO2 contents (Fig. 8), and weak negative P anom-alies (Fig. 9b) result from apatite separation. All these characteris-tics suggest the combined processes of crustal assimilation and/orcontamination and fractional crystallization (AFC) in the petrogen-esis of the two earlier intrusions.

The monzogranites of the younger XI have distinct whole-rockgeochemistry, Sr–Nd isotopes and zircon Hf isotopic compositionsfrom those of the two early intrusions (SI and QI), apparentlyreflecting distinct sources or petrogenetic processes, or both. Themonzogranites have relatively low MgO, Cr and Ni contents at highsilica concentrations (Table 2). Their geochemical characteristicscorrespond to the experimental results of partial melting of crustalbasalt compositions (Patiño Douce, 1995; Rapp and Watson, 1995),indicating a crustal source. The Nb/Ta values (av. 7.2) for the monz-ogranites are less than that of mantle-derived melts (17.5 ± 2.0)(Green, 1995), also indicative of a crustal source. The monzogra-nites have slightly negativeeNd(t) values (�2.3 to�2.5) and positivezircon eHf(t) values (+1.3 to +4.6), indicating more addition of juve-nile components than in the two early intrusions. The higher SiO2

and K2O + N2O contents, and depletion of Eu, P and Ti are similar toother Early Cretaceous Xiaochengzi granitoids in the belt (Liu et al.,2005). When combined with similar Nd isotope and zircon Hf iso-tope, this indicates a common source and suggests that the intru-sion was sourced from evolved and differentiated magmas. Thehigh K contents indicate a K-bearing phase, such as amphibole or

ri Sm(ppm)

Nd(ppm)

147Sm/144Nd 143Nd/144Nd 2r fSm/Nd eNd(t) TDM

(Ga)

.7058 4.31 22.30 0.1166 0.512400 7 �0.41 �3.2 1.18

.7058 4.96 25.50 0.1177 0.512475 7 �0.40 �1.8 1.07

.7058 4.94 26.10 0.1143 0.512376 8 �0.42 �3.7 1.19

.7057 6.18 30.20 0.1235 0.512470 6 �0.37 �2.0 1.15

.7061 4.87 27.60 0.1068 0.512446 8 �0.46 �2.3 1.00

.7060 4.85 28.40 0.1032 0.512432 5 �0.48 �2.5 0.99

147Sm/144Nd)CHUR � 1, where s = sample, (143Nd/144Nd)CHUR = 0.512638, andr isotopic ratio growth equation: TDM = 1/k � ln(1 + ((143Nd/144Nd)s � 0.51315)/

Table 4Zircon Hf isotopic analyses for the Renjiayingzi pluton in southern Inner Mongolia, China.

Sample no. t (Ma) 176Yb/177Hf 176Lu/177Hf 176Hf/177Hf 2rm eHf(0) eHf(t) 2s TDM1(Hf) (Ga) fLu/Hf TDM2(Hf) (Ga)

11RJ-2 pyroxene diorite1 138 0.105509 0.001887 0.282681 34 �3.2 �0.4 1.2 0.83 �0.943 1.222 138 0.137758 0.002290 0.282670 27 �3.6 �0.8 0.9 0.85 �0.931 1.243 138 0.110310 0.002533 0.282865 37 3.3 6.1 1.3 0.57 �0.924 0.804 138 0.125526 0.002002 0.282759 27 �0.5 2.4 1.0 0.72 �0.94 1.045 138 0.138453 0.002230 0.282738 36 �1.2 1.6 1.3 0.75 �0.933 1.096 138 0.128939 0.002293 0.282857 29 3.0 5.8 1.0 0.58 �0.931 0.827 138 0.106223 0.001932 0.282765 30 �0.2 2.6 1.1 0.71 �0.942 1.038 138 0.070733 0.001290 0.282697 29 �2.6 0.3 1.0 0.79 �0.961 1.189 138 0.117105 0.002164 0.282737 28 �1.2 1.6 1.0 0.75 �0.935 1.09

10 138 0.092532 0.001737 0.282731 25 �1.5 1.4 0.9 0.75 �0.948 1.1011 138 0.066711 0.001816 0.282763 29 �0.3 2.5 1.0 0.71 �0.945 1.0312 138 0.080813 0.002114 0.282711 29 �2.2 0.7 1.0 0.79 �0.936 1.1513 138 0.091144 0.001573 0.282749 30 �0.8 2.1 1.1 0.72 �0.953 1.06

11RJ-11 monzogranite1 126 0.042351 0.000947 0.282816 20 1.5 4.2 0.7 0.62 �0.97 0.912 126 0.096176 0.002126 0.282766 26 �0.2 2.4 0.9 0.71 �0.94 1.033 126 0.035678 0.000673 0.282790 25 0.6 3.3 0.9 0.65 �0.98 0.974 126 0.038893 0.000775 0.282825 24 1.9 4.6 0.8 0.60 �0.98 0.895 126 0.031628 0.000749 0.282731 22 �1.4 1.3 0.8 0.73 �0.98 1.106 126 0.058838 0.001107 0.282769 24 �0.1 2.6 0.8 0.69 �0.97 1.027 130 0.075539 0.001397 0.282717 27 �2.0 0.8 1.0 0.77 �0.96 1.148 135 0.023804 0.000447 0.282718 25 �1.9 1.0 0.9 0.75 �0.99 1.139 142 0.035112 0.000622 0.282750 23 �0.8 2.3 0.8 0.70 �0.98 1.05

10 133 0.054003 0.001089 0.282824 22 1.8 4.7 0.8 0.61 �0.97 0.8911 135 0.061099 0.001091 0.282796 19 0.9 3.7 0.7 0.65 �0.97 0.9512 138 0.046089 0.000824 0.282824 25 1.9 4.8 0.9 0.60 �0.98 0.8913 134 0.023546 0.000470 0.282747 22 �0.9 2.0 0.8 0.71 �0.99 1.0614 139 0.026292 0.000556 0.282723 24 �1.7 1.3 0.8 0.74 �0.98 1.1115 134 0.048437 0.000905 0.282717 25 �2.0 0.9 0.9 0.76 �0.97 1.13

Note: eHf(0) = ((176Hf/177Hf)/(176Hf/177Hf)CHUR,0 � 1) � 10,000, fLu/Hf = (176Lu/177Hf)/(176Lu/177Hf)CHUR � 1. eHf(t) = ((176Hf/177Hf)s � (176Lu/177Hf)s � (ekt � 1))/((176Hf/177Hf)CHUR,0 � (176Lu/177Hf)CHUR � (ekt � 1)) � 1) � 10,000. TDM1(Hf) = 1/k � (1 + ((176Hf/177Hf)s � (176Hf/177Hf)DM)/((176Lu/177Hf)s � (176Lu/177Hf)DM)).TDM2(Hf) = TDM1(Hf) � (TDM1(Hf) � t)((fCC � fS)/(fCC � fDM)); where, (176Lu/177Hf)s and (176Hf/177Hf)s are the measured values of samples; (176Lu/177Hf)CHUR = 0.0332 and(176Hf/177Hf)CHUR,0 = 0.282772; (176Lu/177Hf)DM = 0.0384 and (176Hf/177Hf)DM = 0.28325; fCC = �0.548 (average continental crust), fDM = 0.16, t = crystallization time of zircon,k = 1.865 � 10�11 yr�1 reported by Scherer et al. (2001) used in calculation.

Fig. 11. eHf(t) vs. age diagram for the Renjiayingzi pluton. Data for the EarlyCretaceous Xiaochengzi pluton and Proterozoic gneisses in this belt and the EarlyCretaceous granitoids in the northern continental block are from Liu et al. (2009).


phlogopite in their source. The higher Rb/Sr (0.4–0.5) and lower Ba/Rb (4.2–6.0) ratios are consistent with melts in equilibrium withphlogopite (Furman and Graham, 1999). Moreover, the moderatelyhigh (La/Yb)N ratios (Table 2), combined with relatively low HREEabundances of the monzogranites (Fig. 9a), suggest that garnetmay be a residual phase in their source. Melting of juvenile crustalrocks resulting from mafic magma underplating, with a significantconcentration of Ca, Mg and Fe under elevated pressure, wouldproduce residual clinopyroxene and garnet, and consequently

enrich partial melts in SiO2, making them more granitic(Litvinovsky et al., 2000). The XI samples show moderate negativeEu anomalies (dEu from 0.59 to 0.76) in the chondrite-normalizedrare earth element diagrams (Fig. 9a) and weak depletion in Ba inthe primitive mantle-normalized trace element diagram (Fig. 9b),indicative of plagioclase fractionation. This is also supported bythe Rb/Sr and Ba vs. Sr diagrams (Figs. 12c and 12d). The enrich-ment in Th in the primitive mantle-normalized trace element dia-gram (Fig. 9b) suggests an accumulation of accessory zircon in themonzogranites, whereas the depletions in P and Ti reveal progres-sive removal of apatite and Ti-bearing phases (ilmenite, titanite,etc.). Therefore, the geochemical features and zircon Hf isotopiccompositions indicate that the primary parental magma of themonzogranites was derived from juvenile crust via plagioclase-dominated fractional crystallization, with minor accessory mineraldepletion.

Rocks of the Early Cretaceous Renjiayingzi pluton contain someMiddle Triassic inherited zircons, indicating an earlier magmaticepisode as a precursor to the dioritic magma-generating event inthe source region. On the northern side of the Solonker–Xar Moronsuture zone, voluminous end-Permian to Middle Triassic (253–229 Ma) igneous rocks record the final stages of magmatism re-lated to closure of the paleo-Asian Ocean in the eastern CAOB(Fig. 1; Li et al., 2007, 2010; Chen et al., 2009; Liu et al., 2009,2012; Jian et al., 2010; Wu et al., 2011). In the eastern CAOB, volu-minous post-orogenic granites were intruded during the LateTriassic to Early Jurassic, with ages of 212–190 Ma (Wu et al.,2002, 2011; Li et al., 2010). Liu et al. (2009) provided some insightinto why the granitic zircon eHf(t) values decrease to more chon-dritic values during the period 146–125 Ma, proposing that sourcecompositions in the lower crust likely experienced a change as the

Fig. 12. (a) Ni and (b) V vs. Cr, (c) Rb/Sr and (b) Ba vs. Sr diagrams showing crystal fractionation trends involved in the petrogenesis of the Early Cretaceous Renjiayingzipluton in southern Inner Mongolia. Partition coefficients are from Rollison (1993). Symbols as in Fig.7.


result of mafic magma underplating. Eventually, the underplatedmafic rocks became the dominant source component (Liu et al.,2009). SHRIMP zircon U–Pb dating from the Hegenshan mafic–ultramafic massifs between the southern Mongolia active conti-nental margin and the northern continental block (Fig. 1) yieldages of 139–125 Ma, indicating the occurrence of an Early Creta-ceous mantle-melting episode in the region (Jian et al., 2012). Asa response to this event, the coeval Renjiayingzi intermediate-acidmagmatism may also be attributed to mantle-derived magmaticunderplating, resulting from asthenospheric upwelling in responseto lithospheric extension in the southern CAOB. This geodynamicprocess is also evidenced by extensional basins and metamorphiccore complexes in Inner Mongolia, which were initiated in the LateJurassic but became widespread in the Early Cretaceous (Meng,2003; Davis et al., 2009; Lin et al., 2011; Wang et al., 2011, 2012).

6.3. An incremental emplacement and growth model

Plutons are generally built rapidly in large magma chambers(e.g., Paterson and Vernon, 1995; Petford et al., 2000). A largepluton should cool and solidify in less than 1 m.y. (Menand,2008) if it is assumed that it was emplaced during a single discreteigneous event. Field relations and our reported new zircon U–Pbages show that the Renjiayingzi pluton contains at least threemagmatic additions over a 10 m.y. interval between 138 Ma and126 Ma. Therefore, we propose an incremental emplacement andgrowth model to explain the development of the Renjiayingzhipluton.

6.3.1. Structural control and emplacement mechanismRegional structural features in the area are characterized by NE–

SW-trending foliations and faults (Fig. 2). The east–west-trending

Xar Moron suture zone in the south is the most important deep faultzone in the region, recording the final amalgamation of the southernmargin of the Siberia craton with the North China Craton (Li, 2006;Jian et al., 2010). A widespread NE–SW-trending granitic beltcontaining many Cretaceous granitoid intrusions also characterizesthis zone (Fig. 2).

The Renjiayingzi pluton is composed of three small intrusionsthat are young from NW to SE and appear to be superimposed overeach other (Fig. 3). Internal contacts are distinguishable and reflectchanges in petrographic characteristics, with the relation betweenthe QI and the XI being a sharp intrusive contact due to magmainjection. Where the intrusions directly contact Permian clasticrocks, a distinct thermal aureole has developed, producing hornfel-ses (Fig. 3).

Plutons are commonly emplaced in tectonically active settingsand ascend into the upper crust where fracturing of wall-rock isa major mechanical process (Hutton, 1992; Cruden, 1998; Bartleyet al., 2008; Weinberg and Regenauer-Lieb, 2010). Pre-existingductile shear zones or deep faults along the Xar Moron suture zoneprobably played a critical role in the emplacement of theRenjiayingzi pluton (BGMRIM, 1995, 1996; Wang et al., 1999).Permian–Cretaceous granitoid intrusions to the north of the XarMoron fault zone extend in a northeast direction (Fig. 2), indicatingthat deep faults with this trend probably provided a conduit andfacilitated the ascent of magmas that were sourced at deeper crus-tal levels. The ENE–WSW-striking dextral ductile shear to thesoutheast of the Renjiayingzi pluton apparently controlled thespatial distribution and location of each intrusion (Fig. 3). Becausetectonic dilation is the dominant space-making mechanism duringemplacement of a pluton (e.g., Brooks Hanson and Glazner, 1995;Platten, 2000; Vogel et al., 2001; Gerbi et al., 2004; Bartley et al.,2008), dextral ductile shearing would have formed tensile cracks


that continued to open, thus providing a conduit for the three dis-crete and relatively small repeated magma pulses over an intervalof ca. 10 m.y.

An increasing number of studies have shown that a significantnumber of crustal plutons are fed and amalgamated by one ormore dykes, sills, conduits or tubes (e.g., Coleman et al., 2004;Glazner et al., 2004; Menand, 2008; Horsman et al., 2009; Paterson,2009). We propose that the magmas of the two early injections (SIand QI) and the late intrusion (XI) were emplaced at slightly differ-ent crustal levels, in harmony with the current distribution pattern(Fig. 3). In general, ascent of magmas from deeper crustal levels ismore diffuse, whereas magmas emplaced into shallow crust be-come more localized due to their higher density and viscosity.The early SI was produced at a somewhat deeper level and itsemplacement was controlled by the space provided by dextralENE–WSW shearing, allowing it to ascend and subsequentlyformed inward-dipping magmatic foliations due to the relativerigidity of the country rocks. Later magma forming the QI reacheda slightly shallower crustal level and formed both outward- and in-ward-dipping magmatic foliations. The shearing probably pro-duced ring-like fractures along the margins of the earlyintrusions and provided space for ascent of magma that formedthe XI with its almost circular shape.

6.3.2. Incremental growth modelZonation patterns in plutons have been proposed to result

mainly from in situ crystal fractionation (e.g., Bateman and Chap-pell, 1979; Tindle and Pearce, 1981; Mahood et al., 1996) or mag-ma mixing (e.g., Kistler et al., 1986; Frost and Mahood, 1987).However, plutons emplaced in the upper crust rarely experiencefractionation and magma mixing (Coleman et al., 2004; Glazneret al., 2004; Miller, 2008; Annen, 2009). Instead, a growing bodyof evidence indicates that some, and perhaps most, plutons growincrementally by relatively small repeated magma pulses (e.g.Coleman et al., 2004; Glazner et al., 2004; Matzel et al., 2006;Walker et al., 2007; Burgess and Miller, 2008; Michel et al., 2008;Miller, 2008; Miller et al., 2011; Paterson et al., 2011). Diapirism,ballooning and stoping with large frozen magma chambers are of-ten considered as the main emplacement mechanisms of plutons(e.g., Paterson and Vernon, 1995; Pitcher, 1997; Wang et al.,2000; Gerbi et al., 2004; He et al., 2009; Paterson, 2009; Patersonet al., 2012).

As discussed above, the Renjiayingzi pluton was formed bythree discrete magma injections. It lacks the steeply outward-dip-

Fig. 13. Schematic diagrams showing upward-building model of incremental growth forthe text for detailed explanation.

ping concentric magmatic foliations and radial steeply-plungingstretching lineations typical of magmatic ballooning and diapirism(Clemens, 1998; England, 1990; Paterson and Vernon, 1995; Heet al., 2009). The weak magmatic foliations, the absence of flatten-ing strain at the margins of the pluton and weak ductile deforma-tion of the host rocks (BGMRIM, 1995), indicate diapirism andballooning were not the main emplacement mechanism. However,without exposure of the pluton floor and geophysical data, therewill always remain some ambiguity in the regard. Based on theabove considerations, a mechanism of fracture-based magmaticcrack-sealing may represent a more plausible intrusive mechanism(Bartley et al., 2008).

The younging of magmatism in the Renjiayingzi pluton indi-cates the locus was shifting to the ESE over time (Fig. 3). As sum-marized by Kavanagh et al. (2006), Bartley et al. (2008) andMenand (2008), styles of incremental emplacement may includeover-accretion, under-accretion, and middle-accretion, dependingon the relative rigidities of the country rocks and the early intru-sions that formed the growing igneous body (Menand, 2008).Younger magma may accumulate either on top of older intrusions(over-accretion) or underneath them (under-accretion) (Wiebe andCollins, 1998; Galerne et al., 2008), broadly similar to the so-called‘‘upward-building’’ or ‘‘downward-building’’ growth model of Bart-ley et al. (2008). Subsequently, middle-accretion can also occur,whereby a new intrusion is injected in between previously em-placed intrusions (Kavanagh et al., 2006; Bartley et al., 2008).

We therefore propose that the Renjiayingzi pluton was built byover-accretion or upward stacking (Fig. 13). Dykes commonly rep-resent feeders of such composite plutons, which grew by injectionof magma into dilatant cracks (Glazner and Bartley, 2006; Bartleyet al., 2008). Due to crack opening, magma ascends to the emplace-ment level along dyke conduits and, once formed, the pluton doesnot ascend farther. Pluton emplacement by opening and filling ofcracks is also compatible with slow pluton growth (up to 10 m.y.in this case). Incremental upward building helps retain thermal en-ergy and maintain a high temperature in the pluton, which facili-tates subsequent increments of generally similar dimensions. Theroof of each intrusion bulged (or was uplifted) due to verticalexpansion of the intrusion (Fig. 13). Vertical bulging or upliftingof the roof was facilitated by the thermal effect on the overlyingrocks due to vertical heat flow and over-pressure of the magmas(Pollard and Muller, 1976; Cruden et al., 2006).

The Renjiayingzi pluton only crops out over a small area, and itsdimensions appear to be much smaller than in other studies

the Renjiayingzi pluton by amalgamation of three repeated small magma pulses. See


reported in the literature. However it is similar to the upward-build-ing Alta stock in the Wasatch Range, Utah (Bartley et al., 2008). deSaint Blanquat et al. (2011) proposed a positive correlation betweenpluton size and duration of pluton construction, although small andvery slowly-emplaced plutons (less than ca.100 km3 in more than100,000 years) have not been identified to date. However, theRenjiayingzi pluton provides an opportunity to test a paradigm fora small pluton showing protracted magmatic emplacement (ca.10 m.y.). The QI was emplaced into the earlier SI with similar volumein an upward-building mode in less than 4 m.y., whereas the XI cutthe QI in a similar manner ca. 5 m.y. later (Fig. 13).

Pitcher (1997) recognized multi-pulse plutonic systems thatwere emplaced over a significant time span, but stated that ‘‘theentire magmatic life of a multipulse pluton may not exceed amillion years.’’ Similarly, modeling by Petford et al. (2000) indicatedtimescales of less than 100,000 years for most large plutons. How-ever, plutons may take millions of years to grow, such that differentparts of a pluton, mapped as a single intrusion, differ substantiallyin age (e.g., Coleman et al., 2004; Matzel et al., 2006; Bartley et al.,2008; Annen, 2011; Miller et al., 2011; Paterson et al., 2011). Ourdata also indicate a magmatic lifetime of over 10 m.y. for theRenjiayingzi pluton. The data are of key significance to a betterunderstanding of magmatic processes and pluton construction.

7. Conclusions

The Renjiayingzi pluton approximates an oval shape and occu-pies a total area of 4.5 km2. It consists of the Shuangjianshan pyrox-ene diorite Intrusion (SI) in the NW, the Qianweiliansu tonaliteIntrusion (QI) to the E, and the Xingshuwabeishan monzograniteIntrusion (XI) to the ESE. These intrusions were dated at138 ± 1 Ma, 134 ± 2 Ma and 126 ± 1 Ma, respectively, by zirconU–Pb methods, establishing a younging to the ESE. These results,combined with contrasting textures and geochemical compositionsof each intrusion, as well as contact relations, indicate the entireRenjiayingzi pluton was built and developed through three separatemagmatic pulses over a period of 10 m.y. The early pyroxene dioriteof the SI and the tonalite of the QI are close in U–Pb age and showsimilar geochemical characteristics. They most likely evolved fromthe same magma source and underwent similar petrogenetic pro-cesses. They have high MgO concentrations at low silica contents,are enriched in large ion lithophile (LILEs), depleted in high fieldstrength elements (HFSEs), negative eNd(t) values (�1.8 to �3.7),with Nd model ages of 1.07–1.19 Ga and variable zircon eHf(t) values(�0.8 to +6.1) for the pyroxene diorite of the SI, indicating that theywere mainly derived from juvenile crust with some old crustal con-tribution and clinopyroxene-dominated fractional crystallization.However, the weak negative eNd(t) values (�2.3 to �2.5), youngNd model ages (0.99–1.00 Ga), positive zircon eHf(t) values (+1.3to +4.6), high SiO2 and K2O + N2O contents, and depleted Eu, P andTi characteristics of the monzogranite from the late XI indicate thatthis intrusion was derived from a different source. The monzogra-nites were the result of partial melting of juvenile crust in responseto mantle-derived mafic magma underplating, accompanied byplagioclase-dominated fractional crystallization.

An incremental growth model by amalgamation of repeatedsmall magma pulses is proposed to explain the emplacementmechanism of the Renjiayingzi pluton. The younging to the ESEmost likely reflects emplaced by upward stacking, building onthe space created by previous uplifting of the roof. The pluton is lo-cated in the ENE–WSW-trending Xar Moron suture zone and it islikely that pre-existing deep-crustal dextral faults controlled initialemplacement in a post-collisional or post-orogenic setting. Thisstudy demonstrates how a small composite pluton can developover a protracted period of 10 m.y.

Acknowledgments

We thank Dr. Xuance Wang for his comments and suggestionsfor improving the manuscript. We are grateful to Dr. Kejun Houand Xingjun Shi for their laboratory assistance for zircon Hf analy-ses. We also thank Adam Frew for assistance with the SHRIMPzircon U–Pb dating. We greatly appreciate the helpful reviewsand comments from associate editor Profs. M. Santosh, WenjiaoXiao and Shuanhong Zhang, which helped to improve and clarifythe presentation. This research was supported financially by theGeological Survey of China (Grant Nos. 1212010611808 and1212011120135), and the Major State Basic Research Program ofthe P.R. China (Grant 2013CB429803), and is The Institute forGeoscience Research (TIGeR) publication umber 473.

Appendix A. Supplementary material

Supplementary data associated with this article can be found, inthe online version, at http://dx.doi.org/10.1016/j.jseaes.2013.07.005.

References

Andersen, T., 2002. Correction of common lead in U–Pb analyses that do not report204Pb. Chemical Geology 192, 59–79.

Annen, C., 2009. From plutons to magma chambers: thermal constraints on theaccumulation of eruptible silicic magma in the upper crust. Earth and PlanetaryScience Letters 284, 409–416.

Annen, C., 2011. Implications of incremental emplacement of magma bodies formagma differentiation, thermal aureole dimensions and plutonism–volcanismrelationships. Tectonophysics 500, 3–10.

Badarch, G., Cunningham, W.D., Windley, B.F., 2002. A new terrane subdivision forMongolia: implications for the Phanerozoic crustal growth of Central Asia.Journal of Asian Earth Sciences 21, 87–110.

Bartley, J.M., Coleman, D.S., Glazner, A.F., 2008. Incremental pluton emplacement bymagmatic crack-seal. Transactions of the Royal Society of Edinburgh – EarthSciences 97, 383–396.

Bateman, P.C., Chappell, B.W., 1979. Crystallization, fractionation, and solidificationof the Tuolumne Intrusive Series, Yosemite National Park, California. GeologicalSociety of America Bulletin 90, 465–482.

BGMRIM, 1991. Regional geology of Inner Mongolia Autonomous Region. GeologicalPublishing House, Beijing, 726pp (in Chinese).

BGMRIM, 1995. Geological Map of the Renjiayingzi Region, Inner Mongolia of China,1:50,000 (in Chinese).

BGMRIM, 1996. Rock and Stratum of Inner Mongolia Autonomous Region. ChinaUniversity of Geosciences Press, Wuhan, 344pp (in Chinese).

Bialas, R.W., Buck, W.R., Qin, R., 2010. How much magma is required to rift acontinent? Earth and Planetary Science Letters 292, 68–78.

Brooks Hanson, R., Glazner, A.F., 1995. Thermal requirements for extensionalemplacement of granitoids. Geology 23, 213–216.

Burgess, S.D., Miller, J.S., 2008. Construction, solidification and internaldifferentiation of a large felsic arc pluton: cathedral peak granodiorite, SierraNevada Batholith. Geological Society, London, Special Publications 304, 203–233.

Chen, B., Jahn, B.M., Wilde, S., Xu, B., 2000. Two contrasting Paleozoic magmaticbelts in northern Inner Mongolia, China: petrogenesis and tectonic implications.Tectonophysics 328, 157–182.

Chen, B., Jahn, B.M., Tian, W., 2009. Evolution of the Solonker suture zone:constraints from zircon U–Pb ages, Hf isotopic ratios and whole-rock Nd–Srisotope compositions of subduction- and collision-related magmas and forearcsediments. Journal of Asian Earth Sciences 34, 245–257.

Clemens, J.D., 1998. Observations on the origins and ascent mechanisms of graniticmagmas. Journal of the Geological Society 155, 843–851.

Coleman, D.S., Gray, W., Glazner, A.F., 2004. Rethinking the emplacement andevolution of zoned plutons: geochronologic evidence for incremental assemblyof the Tuolumne Intrusive Suite, California. Geology 32, 433–436.

Cruden, A.R., 1998. On the emplacement of tabular granites. Journal of theGeological Society 155, 853–862.

Cruden, A.R., Tobisch, O.T., Launeau, P., 2006. Emplacement and growth of plutons:implications for rates of melting and mass transfer in continental crust. In:Brown, M., Rushmer, T. (Eds.), Evolution and Differentiation of the ContinentalCrust. Cambridge University Press, New York, pp. 455–519.

Davis, G.A., Meng, J.F., Cao, W.R., Du, X.Q., 2009. Triassic and Jurassic Tectonics in theEastern Yanshan Belt, North China: insights from the ControversialDengzhangzi Formation and its neighboring units. Earth Science Frontiers 16,69–86.

Davis, J.W., Coleman, D.S., Gracely, J.T., Gaschnig, R., Stearns, M., 2012. Magmaaccumulation rates and thermal histories of plutons of the Sierra Nevadabatholith, CA. Contributions to Mineralogy and Petrology 163, 449–465.



http://refhub.elsevier.com/S1367-9120(13)00352-0/h0005
























































de Saint Blanquat, M., Horsman, E., Habert, G., Morgan, S., Vanderhaeghe, O., Law, R.,Tikoff, B., 2011. Multiscale magmatic cyclicity, duration of pluton construction,and the paradoxical relationship between tectonism and plutonism incontinental arcs. Tectonophysics 500, 20–33.

England, R.W., 1990. The identification of granitic diapirs. Journal of the GeologicalSociety 147, 931–933.

Frost, B.R., Frost, C.D., 2008. A geochemical classification for feldspathic igneousrocks. Journal of Petrology 49, 1955–1969.

Frost, T.P., Mahood, G.A., 1987. Field, chemical, and physical constraints on mafic–felsic magma interaction in the Lamarck Granodiorite, Sierra Nevada, California(USA). Geological Society of America Bulletin 99, 272–291.

Frost, B.R., Barnes, C.G., Collins, W.J., Arculus, R.J., Ellis, D.J., Frost, C.D., 2001. Ageochemical classification for granitic rocks. Journal of Petrology 42, 2033–2048.

Furman, T., Graham, D., 1999. Erosion of lithospheric mantle beneath the EastAfrican Rift system: geochemical evidence from the Kivu volcanic province.Lithos 48, 237–262.

Galerne, C.Y., Neumann, E.R., Planke, S., 2008. Emplacement mechanisms of sillcomplexes: information from the geochemical architecture of the Golden ValleySill Complex, South Africa. Journal of Volcanology and Geothermal Research177, 425–440.

Gerbi, C., Johnson, S.E., Paterson, S.R., 2004. Implications of rapid, dike-fed plutongrowth for host-rock strain rates and emplacement mechanisms. Journal ofStructural Geology 26, 583–594.

Glazner, A.F., Bartley, J.M., 2006. Is stoping a volumetrically significant plutonemplacement process? Bulletin of the Geological Society of America 118, 1185–1195.

Glazner, A.F., Bartley, J.M., Coleman, D.S., Gray, W., Taylor, R.Z., 2004. Are plutonsassembled over millions of years by amalgamation from small magmachambers? GSA Today 14, 4–11.

Green, T.H., 1995. Significance of Nb/Ta as an indicator of geochemical processes inthe crust-mantle system. Chemical Geology 120, 347–359.

He, B., Xu, Y.G., Paterson, S., 2009. Magmatic diapirism of the Fangshan pluton,southwest of Beijing, China. Journal of Structural Geology 31, 615–626.

Horsman, E., Morgan, S., De Saint-Blanquat, M., Habert, G., Nugent, A., Hunter, R.A.,Tikoff, B., 2009. Emplacement and assembly of shallow intrusions from multiplemagma pulses, Henry Mountains, Utah. Earth and Environmental ScienceTransactions of the Royal Society of Edinburgh 100, 117–132.

Howard, K.A., Wooden, J.L., Barnes, C.G., Premo, W.R., Snoke, A.W., Lee, S.Y., 2011.Episodic growth of a Late Cretaceous and Paleogene intrusive complex ofpegmatitic leucogranite, Ruby Mountains core complex, Nevada, USA.Geosphere 7, 1220–1248.

Hutton, D.H.W., 1992. Granite sheeted complexes: evidence for the dyking ascentmechanism. Transactions – Royal Society of Edinburgh: Earth Sciences 83, 377–382.

Jahn, B.M., Wu, F.Y., Chen, B., 2000. Granitoids of the Central Asian orogenic belt andcontinental growth in the Phanerozoic. Transactions of the Royal Society ofEdinburgh, Earth Science 91, 181–193.

Jahn, B.M., Windley, B., Natal’in, B., Dobretsov, N., 2004. Phanerozoic continentalgrowth in Central Asia. Journal of Asian Earth Sciences 23, 599–603.

Jahn, B.M., Litvinovsky, B.A., Zanvilevich, A.N., Reichow, M., 2009. Peralkalinegranitoid magmatism in the Mongolian–Transbaikalian Belt: evolution,petrogenesis and tectonic significance. Lithos 113, 521–539.

Jian, P., Liu, D.Y., Kröner, A., Windley, B.F., Shi, Y.R., Zhang, F.Q., Shi, G.H., Miao, L.C.,Zhang, W., Zhang, Q., Zhang, L.Q., Ren, J.S., 2008. Time scale of an early to mid-Paleozoic orogenic cycle of the long-lived Central Asian Orogenic Belt, InnerMongolia of China: implications for continental growth. Lithos 101, 233–259.

Jian, P., Liu, D.Y., Kröner, A., Windley, B.F., Shi, Y.R., Zhang, W., Zhang, F.Q., Miao, L.C.,Zhang, L.Q., Tomurhuu, D., 2010. Evolution of a Permian intraoceanic arc–trenchsystem in the Solonker suture zone, Central Asian Orogenic Belt, China andMongolia. Lithos 118, 169–190.

Jian, P., Kröner, A., Windley, B.F., Shi, Y.R., Zhang, W., Zhang, L.Q., Yang, W.R., 2012.Carboniferous and Cretaceous mafic–ultramafic massifs in Inner Mongolia(China): a SHRIMP zircon and geochemical study of the previously presumedintegral ‘‘Hegenshan ophiolite’’. Lithos 142–143, 48–66.

Jiang, S.H., Ling, Q.L., Liu, Y.F., Liu, Y., 2012. Zircon U–Pb ages of the magmatic rocksoccurring in and around the Dajing Cu–Ag–Sn polymetallic deposit of InnerMongolia and contrains to the ore-forming age. Acta Perologica Sinica 28, 495–513 (in Chinese with English abstract).

Kavanagh, J.L., Menand, T., Sparks, R.S.J., 2006. An experimental investigation of sillformation and propagation in layered elastic media. Earth and Planetary ScienceLetters 245, 799–813.

Kistler, R.W., Chappell, B.W., Peck, D.L., Bateman, P.C., 1986. Isotopic variation in theTuolumne Intrusive Suite, central Sierra Nevada, California. Contributions toMineralogy and Petrology 94, 205–220.

Kovalenko, V.I., Yarmolyuk, V.V., Kovach, V.P., Kotov, A.B., Kozakov, I.K., Salnikova,E.B., Larin, A.M., 2004. Isotopic provinces, mechanism of generation and sourcesof the continental crust in the Central Asian mobile belt: geological and isotopicevidence. Journal of Asian Earth Sciences 23, 605–627.

Kravchinsky, V.A., Cogne, J.P., Harbert, W.P., Kuzmin, M.I., 2002. Evolution of theMongol–Okhotsk Ocean as constrained by new palaeomagnetic data from theMongol–Okhotsk suture zone, Siberia. Geophysical Journal International 148,34–57.

Kröner, A., Hegner, E., Lehmann, B., Heinhorst, J., Wingate, M.T.D., Liu, D.Y., Ermelov,P., 2008. Palaeozoic arc magmatism in the Central Asian Orogenic Belt of

Kazakhstan: SHRIMP zircon ages and whole-rock Nd isotopic systematics.Journal of Asian Earth Sciences 32, 118–130.

Kröner, A., Kovach, V., Belousova, E., Hegner, E., Armstrong, R., Dolgopolova, A.,Seltmann, R., Alexeiev, D.V., Hoffmann, J.E., Wong, J., Sun, M., Cai, K., Wang, T.,Tong, Y., Wilde, S.A., Degtyarev, K.E., Rytsk, E., 2013. Reassessment ofcontinental growth during the accretionary history of the Central AsianOrogenic Belt. Gondwana Research. http://dx.doi.org/10.1016/j.gr.2012.12.023.

Li, J.Y., 2006. Permian geodynamic setting of Northeast China and adjacent regions:closure of the Paleo-Asian Ocean and subduction of the Paleo-Pacific Plate.Journal of Asian Earth Sciences 26, 207–224.

Li, J.Y., Gao, L.M., Sun, G.H., Li, Y.P., Wang, Y.B., 2007. Shuangjingzi middle Triassicsyn-collisional crust-derived granite in the east Inner Mongolia and itsconstraint on the timing of collision between Siberian and Sino-Korean paleo-plates. Acta Geologica Sinica 23, 565–582 (in Chinese with English abstract).

Li, J.Y., Zhang, J., Yang, T.N., Li, Y.P., Sun, G.H., Zhu, Z.X., Wang, L.J., 2009. Crustaltectonic division and evolution of the southern part of the North Asian OrogenicRegion and its adjacent areas. Journal of Jilin University (Earth Science Edition)39, 584–605 (in Chinese with English abstract).

Li, S., Wang, T., Tong, Y., 2010. Spatial-temporal distribution and tectonic settings ofEarly Mesozoic granitoids in the middle-south segment of the Central AsiaOrogenic System. Acta Petrologica et Mineralogica 29, 642–662 (in Chinesewith English abstract).

Li, Y.L., Zhou, H.W., Brouwer, F.M., Wijbrans, J.R., Zhong, Z.Q., Liu, H.F., 2011.Tectonic significance of the Xilin Gol Complex, Inner Mongolia, China:petrological, geochemical and U–Pb zircon age constraints. Journal of AsianEarth Sciences 42, 1018–1029.

Lin, W., Monié, P., Faure, M., Schärer, U., Shi, Y., Breton, N.L., Wang, Q., 2011. Coolingpaths of the NE China crust during the Mesozoic extensional tectonics: examplefrom the south-Liaodong peninsula metamorphic core complex. Journal ofAsian Earth Sciences 42, 1048–1065.

Lipman, P.W., 2007. Incremental assembly and prolonged consolidation ofCordilleran magma chambers: evidence from the Southern Rocky Mountainvolcanic field. Geosphere 3, 42–70.

Litvinovsky, B.A., Steele, I.M., Wickham, S.M.I., 2000. Silicic Magma Formation inOverthickened Crust: melting of Charnockite and Leucogranite at 15, 20 and25 kbar. Journal of Petrology 41, 717–737.

Liu, W., Siebel, W., Li, X.J., Pan, X.F., 2005. Petrogenesis of the Linxi granitoids,northern Inner Mongolia of China: constraints on basaltic underplating.Chemical Geology 219, 5–35.

Liu, W., Pan, X.F., Liu, D.Y., Chen, Z.Y., 2009. Three-step continental-crust growthfrom subduction accretion and underplating, through intermediarydifferentiation, to granitoid production. International Journal of Earth Sciences98, 1413–1439.

Liu, Y.S., Wang, X.H., Wang, D.B., He, D.T., Zong, K.Q., Gao, C.G., Hu, Z.C., Gong, H.J.,2012. Triassic high-Mg adakitic andesites from Linxi, Inner Mongolia: insightsinto the fate of the Paleo-Asian ocean crust and fossil slab-derived melt–peridotite interaction. Chemical Geology 328, 89–108.

Long, X., Yuan, C., Sun, M., Safonova, I., Xiao, W.J., Wang, Y., 2012. Geochemistry andU–Pb detrital zircon dating of Paleozoic graywackes in East Junggar, NW China:insights into subductoin–accretion processes in the southern Central AsianOrogenic Belt. Gondwana Research 21, 637–653.

Mahood, G.A., Nibler, G.E., Halliday, A.N., 1996. Zoning patterns and petrologicprocesses in peraluminous magma chambers: Hall Canyon pluton, PanamintMountains, California. Geological Society of America Bulletin 108, 437–453.

Maniar, P.D., Piccoli, P.M., 1989. Tectonic discrimination of granitoids. GeologicalSociety of America Bulletin 101, 635–643.

Matzel, J.E.P., Bowring, S.A., Miller, R.B., 2006. Time scales of pluton construction atdiffering crustal levels: examples from the Mount Stuart and Tenpeakintrusions, North Cascades, Washington. Bulletin of the Geological Society ofAmerica 118, 1412–1430.

Menand, T., 2008. The mechanics and dynamics of sills in layered elastic rocks andtheir implications for the growth of laccoliths and other igneous complexes.Earth and Planetary Science Letters 267, 93–99.

Menand, T., 2011. Physical controls and depth of emplacement of igneous bodies: areview. Tectonophysics 500, 11–19.

Meng, Q.R., 2003. What drove late Mesozoic extension of the northern China–Mongolia tract? Tectonophysics 369, 155–174.

Michaut, C., Jaupart, C., 2011. Two models for the formation of magma reservoirs bysmall increments. Tectonophysics 500, 34–49.

Michel, J., Baumgartner, L., Putlitz, B., Schaltegger, U., Ovtcharova, M., 2008.Incremental growth of the Patagonian Torres del Paine laccolith over 90 k.y.Geology 36, 459–462.

Miller, J.S., 2008. Assembling a pluton. . .one increment at a time. Geology 36, 511–512.

Miller, J.S., Matzel, J.E.P., Miller, C.F., Burgess, S.D., Miller, R.B., 2007. Zircon growthand recycling during the assembly of large, composite arc plutons. Journal ofVolcanology and Geothermal Research 167, 282–299.

Miller, C.F., Furbish, D.J., Walker, B.A., Claiborne, L.L., Koteas, G.C., Bleick, H.A., Miller,J.S., 2011. Growth of plutons by incremental emplacement of sheets in crystal-rich host: evidence from Miocene intrusions of the Colorado River region,Nevada, USA. Tectonophysics 500, 65–77.

Paterson, S.R., 2009. Magmatic tubes, pipes, troughs, diapirs, and plumes: late-stageconvective instabilities resulting in compositional diversity and permeablenetworks in crystal-rich magmas of the Tuolumne batholith, Sierra Nevada,California. Geosphere 5, 496–527.
























































































http://dx.doi.org/10.1016/j.gr.2012.12.023



















































































Paterson, S.R., Vernon, R.H., 1995. Bursting the bubble of ballooning plutons: areturn to nested diapirs emplaced by multiple processes. Geological Society ofAmerica Bulletin 107, 1356–1380.

Paterson, S.R., Okaya, D., Memeti, V., Economos, R., Miller, R.B., 2011. Magmaaddition and flux calculations of incrementally constructed magma chambers incontinental margin arcs: combined field, geochronologic, and thermal modelingstudies. Geosphere 7, 1439–1468.

Paterson, S.R., Memeti, V., Pignotta, G., Erdmann, S., Zák, J., Chambers, J., Ianno, A.,2012. Formation and transfer of stoped blocks into magma chambers: the high-temperature interplay between focused porous flow, cracking, channel flow,host-rock anisotropy, and regional deformation. Geosphere 8, 443–469.

Patiño Douce, A.E., 1995. Experimental generation of hybrid silicic melts by reactionof high-Al basalt with metamorphic rocks. Journal of Geophysical Research:Solid Earth 100, 15623–15639.

Peccerillo, A., Taylor, S.R., 1976. Geochemistry of eocene calc-alkaline volcanic rocksfrom the Kastamonu area, Northern Turkey. Contributions to Mineralogy andPetrology 58, 63–81.

Petford, N., Cruden, A.R., McCaffrey, K.J.W., Vigneresse, J.L., 2000. Granite magmaformation, transport and emplacement in the Earth’s crust. Nature 408, 669–673.

Pitcher, W.S., 1997. The Nature and Origin of Granite, second ed. Chapman & Hall,London, 387pp.

Platten, I.M., 2000. Incremental dilation of magma filled fractures: evidence fromdykes on the Isle of Skye, Scotland. Journal of Structural Geology 22, 1153–1164.

Pollard, D.D., Muller, O.H., 1976. The effect of gradients in regional stress andmagma pressure on the form of sheet intrusions in cross section. Journal ofGeophysical Research 81, 975–984.

Rapp, R.P., Watson, E.B., 1995. Dehydration melting of metabasalt at 8–32 kbar:implications for continental growth and crust-mantle recycling. Journal ofPetrology 36, 891–931.

Rollison, H.R., 1993. Using Geochemical Data: Evaluation, Presentation. LongmanSingapore Publishers, Singapore, Interpretation, 352p.

Scherer, E., Münker, C., Mezger, K., 2001. Calibration of the lutetium–hafnium clock.Science 293, 683–687.

S�engör, A.M.C., Natal’in, B.A., Burtman, U.S., 1993. Evolution of the Altaid tectoniccollage and Paleozoic crustal growth in Eurasia. Nature 364, 209–304.

Sun, S.S., McDonough, W.F., 1989. Chemical and isotopic systematics of oceanicbasalts; implications for mantle composition and processes. Geological SocietySpecial Publications 42, 313–345.

Tindle, A.G., Pearce, J.A., 1981. Petrogenetic modelling of in situ fractionalcrystallization in the zoned Loch Doon pluton, Scotland. Contributions toMineralogy and Petrology 78, 196–207.

Vigneresse, J.L., Bouchez, J.L., 1997. Successive granitic magma batches duringpluton emplacement: the case of Cabeza de Araya (Spain). Journal of Petrology38, 1767–1776.

Vogel, T.A., Cambray, F.W., Constenius, K.N., 2001. Origin and emplacement ofigneous rocks in the central Wasatch Mountains, Utah. Rocky Mountain.Geology 36, 119–162.

Walker Jr., B.A., Miller, C.F., Lowery Claiborne, L., Wooden, J.L., Miller, J.S., 2007.Geology and geochronology of the Spirit Mountain batholith, southern Nevada:implications for timescales and physical processes of batholith construction.Journal of Volcanology and Geothermal Research 167, 239–262.

Wang, Y., Fan, Z.Y., Fang, S., Li, B.Y., 1999. Geological information were discoveredand their plate tectonic significance on the northern bank of Xar Moron river.Geology of Inner Mongolia 90, 6–28 (in Chinese with English abstract).

Wang, T., Wang, X., Li, W., 2000. Evaluation of multiple emplacement mechanisms:the Huichizi granite pluton, Qinling orogenic belt, central China. Journal ofStructural Geology 22, 505–518.

Wang, T., Zheng, Y.D., Zhang, J.J., Zeng, L.S., Donskaya, T., Guo, L., Li, J.B., 2011.Pattern and kinematic polarity of late Mesozoic extension in continental NEAsia: perspectives from metamorphic core complexes. Tectonics 30, TC6007.

Wang, T., Guo, L., Zheng, Y.D., Donskaya, T., Gladkochub, D., Zeng, L.S., Li, J.B., Wang,Y.B., Mazukabzov, A., 2012. Timing and processes of late Mesozoic mid-lower-

crustal extension in continental NE Asia and implications for the tectonicsetting of the destruction of the North China Craton: mainly constrained byzircon U–Pb ages from metamorphic core complexes. Lithos. http://dx.doi.org/10.1016/j.lithos.2012.07.020.

Webb, L.E., Graham, S.A., Johnson, C.L., Badarch, G., Hendrix, M.S., 1999. Occurrence,age, and implications of the Yagan–Onch Hayrhan metamorphic core complex,southern Mongolia. Geology 27, 143–146.

Weinberg, R.F., Regenauer-Lieb, K., 2010. Ductile fractures and magma migrationfrom source. Geology 38, 363–366.

Wiebe, R.A., Collins, W.J., 1998. Depositional features and stratigraphic sections ingranitic plutons: implications for the emplacement and crystallization ofgranitic magma. Journal of Structural Geology 20, 1273–1289.

Windley, B.F., Kröner, A., Guo, J., Qu, G., Li, Y., Zhang, C., 2002. Neoproterozoic toPaleozoic geology of the Altai orogen, NW China: new zircon age data andtectonic evolution. Journal of Geology 110, 719–739.

Windley, B.F., Alexeiev, D., Xiao, W., Kröner, A., Badarch, G., 2007. Tectonic modelsfor accretion of the Central Asian Orogenic Belt. Journal of the GeologicalSociety of London 164, 31–47.

Windley, B.F., Maruyama, S., Xiao, W.J., 2010. Delamination/thinning of sub-continental lithospheric mantle under eastern China; the role of water andmultiple subduction. American Journal of Science 310, 1250–1293.

Wu, F.Y., Sun, D.Y., Li, H.M., Jahn, B.M., Wilde, S.A., 2002. A-type granites innortheastern China: age and geochemical constraints on their petrogenesis.Chemical Geology 187, 143–173.

Wu, F.Y., Sun, D.Y., Ge, W.C., Zhang, Y.B., Grant, M.L., Wilde, S.A., Jahn, B.M., 2011.Geochronology of the Phanerozoic granitoids in northeastern China. Journal ofAsian Earth Sciences 41, 1–30.

Xiao, W.J., Windley, B.F., Hao, J., Zhai, M.G., 2003. Accretion leading to collision andthe Permian Solonker suture, Inner Mongolia, China: termination of the CentralAsian orogenic belt. Tectonics 22, 1069. http://dx.doi.org/10.1029/2002TC1484.

Xiao, W.J., Windley, B.F., Yuan, C., Sun, M., Han, C.M., Lin, S.F., Chen, H.L., Yan, Q.R.,Liu, D.Y., Qin, K.Z., Li, J.L., Sun, S., 2009a. Paleozoic multiple subduction–accretion processes of the southern Altaids. American Journal of Science 309,221–270.

Xiao, W.J., Windley, B.F., Huang, B.C., Han, C.M., Yuan, C., Chen, H.L., Sun, M., Sun, S.,Li, J.L., 2009b. End-Permian to mid-Triassic termination of the accretionaryprocesses of the southern Altaids: implications for the geodynamic evolution,Phanerozoic continental growth, and metallogeny of Central Asia. InternationalJournal of Earth Sciences 98, 1189–1217.

Xiao, W.J., Windley, B.F., Allen, M.B., Han, C., 2013. Paleozoic multiple accretionaryand collisional tectonics of the Chinese Tianshan orogenic collage. GondwanaReseach 23, 1316–1341.

Xu, B., Charvet, J., Chen, Y., Zhao, P., Shi, G.Z., 2012. Middle Paleozoic convergentorogenic belts in western Inner Mongolia (China): framework, kinematics,geochronology and implications for tectonic evolution of the Central AsianOrogenic Belt. Gondwana Research. http://dx.doi.org/10.1016/j.gr.2012.05.015.

Zhang, W., Jian, P., Liu, D.Y., Hou, K.J., 2010. Geochemistry, geochronology and Hfisotopic compositions of Triassic granodiorite-diorite and shoshonite from theDamaoqi area, central Inner Mongolia, China. Geological Bulletin of China 29,821–832 (in Chinese with English abstract).

Zhang, W., Jian, P., Kröner, A., Shi, Y.R., 2012. Magmatic and metamorphicdevelopment of an early to mid-Paleozoic continental margin arc in thesouthernmost Central Asian Orogenic Belt, Inner Mongolia, China. Journal ofAsian Earth Sciences 72, 63–74.

Zhou, J.B., Wilde, S.A., 2012. The crustal accretion history and tectonic evolution ofthe NE China segment of the Central Asian Orogenic Belt. Gondwana Research:doi. http://dx.doi.org/10.1016/j.gr.2012.05.012.

Zhou, J.B., Wilde, S.A., Zhang, X.Z., Zhao, G.C., Zheng, C.Q., Wang, Y.J., Zhang,X.H., 2009. The onset of Pacific margin accretion in NE China: evidence fromthe Heilongjiang high-pressure metamorphic belt. Tectonophysics 478,230–246.

Zorin, Y.A., 1999. Geodynamics of the western part of the Mongolia-Okhotskcollisional belt, Trans-Baikal region (Russia) and Mongolia. Tectonophysics 306,33–56.
































































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