journal of asian earth sciences€¦ · bdepartment of earth sciences, university of adelaide, sa...

Journal of Asian Earth Sciences 113 (2015) 626–643

Contents lists available at ScienceDirect

Journal of Asian Earth Sciences

journal homepage: www.elsevier .com/locate / jseaes

Devonian magmatism associated with arc-continent collision in thenorthern North China Craton: Evidence from the Longwangmiaoultramafic intrusion in the Damiao area

http://dx.doi.org/10.1016/j.jseaes.2015.04.0321367-9120/� 2015 Elsevier Ltd. All rights reserved.

⇑ Corresponding author at: School of Earth Sciences and Resources, ChinaUniversity of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, China.

E-mail address: [email protected] (M. Santosh).

Xueming Teng a, Qiong-Yan Yang a,b, M. Santosh a,b,c,⇑a School of Earth Sciences and Resources, China University of Geosciences Beijing, 29 Xueyuan Road, Beijing 100083, Chinab Department of Earth Sciences, University of Adelaide, SA 5005, Australiac State Key Laboratory of Continental Dynamics, Department of Geology, Northwest University, Xi’an 710069, China

a r t i c l e i n f o

Article history:Received 4 January 2015Received in revised form 16 April 2015Accepted 17 April 2015Available online 14 May 2015

Keywords:Ultramafic intrusionGeochemistryZircon U–Pb geochronologySub-continental lithospheric mantleNorth China craton

a b s t r a c t

The northern margin of the North China Craton (NCC) witnessed extensive felsic and mafic magmatismduring late Paleozoic to early Mesozoic. Here we investigate the ultramafic complex of Longwangmiao inDamiao comprising clinopyroxenite and hornblendite intrusion. The rocks are dominantly composed ofclinopyroxene and hornblende similar to Alaskan-type intrusions. We present zircon U–Pb age data forzircon grains from the hornblendite and clinopyroxenite which show weighted mean 207Pb/206Pb agesof 382 ± 10 Ma and 399.1 ± 4.4 Ma respectively. The hornblendite and clinopyroxenite show similar rareearth element patterns indicating a co-magmatic nature and formation through differentiation and accu-mulation. The parental magma for this intrusion is inferred to be island-arc picrite in composition pos-sibly derived from low degree partial melting of garnet-peridotite facies at the boundary of slightlyenriched sub-continental lithospheric mantle and crust. The hydrous nature of the magma is correlatedwith subduction of the Mongolian oceanic slab beneath the NCC. The magma evolved into basaltic com-position through input of silica-rich crustal components as suggested by the zircon eHf(t) compositionsthat plot between the evolution array of the 2.5–3.0 Ga Neo- to Mesoarchean basement rocks and pre-sumed sub-continental lithospheric mantle array. The enrichment in LILEs (e.g., Rb, K, Ba, Pb, and Sr)and LREEs, and conspicuous depletion of HFSEs (e.g., Nb, Zr, Ti) suggest an Andean-type continentalarc signature. The tectonic setting for the final emplacement of the Devonian intrusion is correlated withthe transformation from arc-related compression to back-arc extension as evidenced by the dual IAB andCRB signature of these rocks. The post-collisional extensional setting might be related to thearc-continent collision between the Bainaimiao arc and the northern NCC during the Late Silurian.

� 2015 Elsevier Ltd. All rights reserved.

1. Introduction

The evolution of sub-continental lithospheric mantle (SCLM)has exerted significant control on the formation of magma systemsand the architecture of the earth’s crust. The nature and composi-tion of the SCLM beneath old cratons is shaped by different cyclesof subduction–accretion and crust–mantle interaction history (e.g.,Santosh, 2010). Magmas sourced from the SCLM have been consid-ered to be tracers of the thermal and physical relationshipsbetween mantle and crust growth, crustal growth, and the natureof lithospheric mantle (Wilson, 1989; Chardon, 2003; Milleret al., 2009; Needy et al., 2009; Zák et al., 2012).

The Central Asian Orogenic Belt (CAOB), located between theSiberian Craton in the north and Tarim-North China Cratons inthe south is considered to represent the largest Phanerozoic accre-tionary orogen in the world (Jahn et al., 2000; Windley et al., 2007;Xiao et al., 2003). The southern CAOB records a prolonged history ofsubduction, accretion and collision of a number of terranes(Mongolian composite terranes) including oceanic plateau, oceanicisland arcs, seamounts, and Precambrian micro-continents (Daviset al., 2001; Xiao et al., 2003, 2014; Hsu et al., 1991; Robinsonet al., 1999; Xu and Chen, 1997; Xiao and Santosh, 2014;Safonova and Santosh, 2014) culminating in the final amalgamationwith the North China Craton along the Solonker suture. However,the process of the amalgamation between the North China Craton(NCC) and the southern Mongolian composite terranes is debated,with different models including southward of Paleo-Asian oceaniclithosphere beneath the NCC (Davis et al., 2001; Xiao et al., 2003),

http://crossmark.crossref.org/dialog/?doi=10.1016/j.jseaes.2015.04.032&domain=pdf

http://dx.doi.org/10.1016/j.jseaes.2015.04.032

mailto:[email protected]


http://www.sciencedirect.com/science/journal/13679120

http://www.elsevier.com/locate/jseaes

X. Teng et al. / Journal of Asian Earth Sciences 113 (2015) 626–643 627

northward subduction beneath successively accreting arc terranes,or continental arc–accretionary complex (Hsu et al., 1991;Robinson et al., 1999). Even some studies do not favor southwardsubduction between the Palaeo-Asian Oceanic crust and theNorth China Craton (eg. Xu and Chen, 1997). The Inner MongoliaPaleo-uplift tectonic unit (IMPU, also called the ‘‘Inner Mongoliaaxis,’’ Huang, 1945; HBGMR, 1989) is an integral component ofthe CAOB. The Archean–Paleoproterozoic high-grade metamorphicrocks and subduction–collision-post collision-related Paleozoicmagmatic rocks exposed along the northern margin of the NCCare considered to represent part of the paleo-uplift fromMeso-Neoproterozoic to early Triassic. The Paleozoic magmaticrocks distributed within the IMPU could provide important cluesto reveal the Paleozoic tectonic process prior to the final amalgama-tion between the NCC and the Mongolian composite terranes andthe nature of the SCLM prior to the Mesozoic destruction of the NCC.

In this study, we present the mineralogical features, major andtrace element data, zircon U–Pb geochronology and Lu–Hf isotopeson the ultramafic intrusion from Longwangmiao in Damiao. Basedon the results, we discuss the petrogenesis and tectonic setting ofthe ultramafic body and attempt to derive constraints on thesub-continental lithospheric mantle and crust–mantle interactionas well as tectonic history of the Mongolian terranes amalgamatedwith the NCC.

2. Geological setting

The NCC (Fig. 1a) is the largest and oldest known cratonicnucleus in China with crustal remnants as old as 3.8 Ga (Liuet al., 1992; Song et al., 1996; Zhai and Santosh, 2011; Zhao andCawood, 2012; Zhao and Zhai, 2013; Zhai, 2014). The Eastern andWestern Blocks of the NCC were amalgamated during latePaleoproterozoic at ca. 1.85 Ga (Zhai and Santosh, 2011, 2013;Yang and Santosh, 2014, 2015; Santosh et al., 2015) marking thefinal cratonization event. After a prolonged period of quiescence,the craton was reactivated along its boundaries andpaleo-sutures with extensive magmatism associated with a seriesof tectonic events including collision of the Yangtze Craton in thesouth in Triassic, the Mesozoic–Cenozoic subduction of Pacificplate underneath the NCC in the east, and the Late Paleozoic south-ward subduction of Paleo-Asian ocean and collision between theMongolian terranes and the NCC, and Early Mesozoic closure ofthe Paleo-Asian ocean and Okhotsk ocean and subsequent forma-tion of the huge accretionary-type Central Asian Orogenic Belt(CAOB) in the north (Tang et al., 2013). The IMPU tectonic unit inthe north and the sub-unit of the Yanshan fold-and-thrust belt inthe south constitute the middle northern margin of the NCC(Fig. 1b).

Our study area Damiao forms part of the IMPU, and is composedof Neoarchean basement rocks intruded by the PaleoproterozoicDamiao gabbro-anorthosite suite (Teng and Santosh, 2015; Zhaoet al., 2009) and unconformably overlain by Jurassic–Cretaceousvolcanic and sedimentary successions (Zhang et al., 2006; Liuet al., 2007). The IMPU is considered to have exhumed during latePaleozoic to early Mesozoic (Zhang et al., 2006; Liu et al., 2007)exposing large tracts of the intrusive rocks including both felsicand mafic bodies with ages ranging from late Paleozoic to earlyMesozoic (HBGMR, 1989; LBGMR, 1989; Pan, 1996; Zhang et al.,2007a,b). These intrusions provide important window to thenature and geochemical characteristics of the SCLM beneath theNCC prior to the Late Mesozoic erosion of the cratonic keel andassociated lithosphere thinning.

The ultramafic intrusion investigated in this study is located inthe northern part of the Paleoproterozoic Damiaogabbro-anorthosite suite (Fig. 2) near the Longwangmiao village.

The ca. 2 km long and 1.5 km wide intrusion is composed of horn-blendite and clinopyroxenite (Fig. 3a) and is emplaced withinNeoarchean metamorphic rocks. The hornblendite and clinopyrox-enite exhibit sharp contact (Fig. 3b). The hornblendites are darkgrayish to black with calcite veins and disseminations (Fig. 3c).The orientation of the hornblende laths is visible in the field andin hand specimen (Fig. 3d), which suggests flow foliation duringmagma ascent.

3. Petrography

Under thin sections, the hornblendite is composed of more than90 vol.% hornblende varying in length from 300 lm to 0.5 mm(Fig. 4a–c). The fine grained hornblendites exhibit little orientationwith interstitial apatite distributed throughout the matrix (Fig. 4b).The common characteristic of the coarse grained hornblendite isthe poikilitic nature of the relative small crystals within the bigcrystals (Fig. 4c). The small, subhedral to anhedralapatites occuras linear arrays filling the fracture of the megacrystic hornblendelaths (Fig. 4c). The clinopyroxenites can be divided into pureclinopyroxenite and hornblende pyroxenite. The pure clinopyrox-eniteis dominated by clinopyroxene (>95 vol.%), with minor horn-blende, apatite and magnetite. Magnetite is interstitial toclinopyroxenes. Apatite occurs as irregular crystals fractureswithin clinopyroxene and magnetite (Fig. 4d). The hornblendeclinopyroxenite is composed of clinopyroxene (80–55 vol.%) andhornblende (15–35 vol.%) with minor olivine, magnetite and apa-tite. The olivine, magnetite and apatite are usually subhedral toanhedral and distributed in the matrix of the hornblende clinopy-roxenite (Fig. 4e). The hornblendite domains adjacent to the calciteveins are intensely altered although they retain the host flow foli-ation. The calcite crystals within the veins are fresh (Fig. 4f). In thisstudy, we collected 12 representative samples, including horn-blendite, pure clinopyroxenite and hornblende clinopyroxenite(the pure clinopyroxenite and hornblende clinopyroxenite aretogether as clinopyroxenite in following text). The summary ofrock types, location with GPS reading, and mineralogy of the sam-ples are given in Table 1.

4. Analytical methods

4.1. Electron microprobe analyses

Electron microprobe analyses of minerals in polished thin sec-tions were carried out on a JEOL JXA-8230 Superprobe at theEMPA Laboratory of Analysis Center of Mineral and Rocks of theInstitute of Mineral Resources, Chinese Academy of GeologicalSciences. Operating conditions were set at 15 kV at 10 nA beamcurrent. Natural minerals and synthetic pure oxides from SPICompany of America were used as standards. For pyroxene, thecalibration standards used were hornblende (for Si, Ti, Al, Fe, Ca,Mg, Na and K), fayalite (for Mn) and Cr2O3 (for Cr). For plagioclase,the standards used were hornblende (for Si, Ti, Al, Fe, Ca, and Mg),albite (for Na), orthoclase (for K), and fayalite (for Mn). Precisionwas better than 1% for element oxides. The results are given inSupplementary Table 1. The spots chosen for electron microscopeanalyses are from fresh domains, excluding the effect of alterationin these minerals.

4.2. U–Pb and Lu–Hf analyses

Zircon separation was performed at the Yu’neng Geological andMineral Separation Survey Centre, Langfang city, Hebei Province,China. The zircon grains were selected by hand picking under thebinocular microscope after gravimetric and magnetic separation

Fig. 1. (a) Schematic map showing the main tectonic units in China and the location of Northern Hebei Domain. (b) Geological outline of Northern Hebei (modified after Liuet al., 2011).

628 X. Teng et al. / Journal of Asian Earth Sciences 113 (2015) 626–643

techniques from rock crushed powder. The grains were mountedonto an epoxy resin discs and then polished to expose the internaltexture. Before U–Pb dating, zircon grains were imaged undertransmitted, reflected light and cathodoluminescence (CL) to checkthe internal textures for choosing the most suitable sites for U–Pbanalyses.

Zircon U–Pb dating and element analyses were carried out on alaser ablation inductively coupled massplasma spectrometry(LA-ICP-MS) housed at National Key Laboratory of ContinentalDynamics of Northwest University, following the analytical proce-dures described by Yuan et al. (2004). In the LA-ICP-MS method,the laser spot diameter and frequency were 30 lm and 10 Hz,respectively. Zircon 91500 was employed as a standard and thestandard silicate glass NIST was used to optimize the instrument.Raw data were processed using the GLITTER program to calculateisotopic ratios and ages of 207Pb/206Pb, 206Pb/238U, 207Pb/235U,respectively (Table 2). Data were corrected for common lead,according to the method of Anderson (2002), and the ages werecalculated by ISOPLOT 4.15 software (Yuan et al., 2004).

In situ zircon Lu–Hf isotopic analyses were conducted on thesame spots or in adjacent domains with same or similar textureswhere for U–Pb dating was done. The analytical procedures fol-lowed those described by Yuan et al. (2008). The energy densityof 15–20 J/cm2 and a spot size of 45 lm were used. The flattest,most stable portions of the signal were selected for analysis.Isobaric interference of 176Lu on 176Hf was adjusted by measuringthe intensity of the interference-free 175Lu isotope and using a rec-ommended 176Lu/175Lu ratio of 0.02669 (DeBievre and Taylor,1993) to calculate 176Lu/177Hf ratios. Adjustment for the isobaricinterference of 176Yb on 176Hf was performed in ‘real time’ as advo-cated by Woodhead et al. (2004), which involved measuring the

interference-free 172Yb and 173Yb during the analyses, calculatingmean bYb value from 172Yb and 173Yb and using the recommended176Yb/172Yb ratio of 0.5886 (Chu et al., 2002). Zircon 91500 wasused as the reference standard with a recommended 176Hf/177Hfratio of 0.282306 ± 10 (Woodhead et al., 2004). All the Lu–Hf iso-tope analysis results were reported with an error of 1r. The decayconstant of 176Lu of 1.865 � 10�11 year�1 was adopted (Schereret al., 2001). Initial 176Hf/177Hf ratios eHf(t) were calculated withreference to the chondritic reservoir (CHUR) of (BlichertToft andAlbarede, 1997) at the time of zircon growth from the magma.Single-stage Hf model age (TDM) was calculated with respect tothe depleted mantle with present-day 176Hf/177Hf = 0.28325 and176Lu/177Hf = 0.0384 (Griffin et al., 2000). Two-stage Hf model age(TDM

C ) was calculated with respect to the average continental crustwith a 176Lu/177Hf ratio of 0.015 (Griffin et al., 2002).

4.3. Whole rock geochemical analyses

Major and trace (including rare earth elements) elements anal-yses were conducted in the National Research Center forGeoanalysis, Beijing. The major elements were determined byX-ray fluorescence (XRF), with an analytical uncertainties rangingfrom 1% to 3%. Loss on ignition was obtained using about 1 g ofsample powder heated at 980 �C for 30 min. The trace elementswere determined as solute by Agilent 7500ce inductively coupledplasma mass spectrometry (ICP-MS). About 50 mg of powder wasdissolved for about 7 days at ca. 100 �C using HF-HNO3 (10:1) mix-tures in screw-top Teflon beakers, followed by evaporation to dry-ness. The material was dissolved in 7 N HNO3 and taken toincipient dryness again, and then was re-dissolved in 2% HNO3 toa sample/solution weight ratio of 1:1000. The analytical errors vary

Fig. 2. Simplified geological map of Damiao area showing the distribution of Phanerozoic mafic–ultramafic intrusions (modified after HBGMR, 1989).


from 5% to 10% depending on the concentration of any given ele-ment. An internal standard was used for monitoring drift duringanalysis; further details are given by Gao et al. (2008).

5. Results

5.1. Mineral chemical characteristics

The analyzed minerals include olivine, clinopyroxene and horn-blende (Supplementary Table 1) and the results are brieflydescribed below.

5.1.1. OlivineOlivine grains from the clinopyroxenite(sample XT24-2) show

FeO content in the range of 16.20–17.59%, and MgO in the rangeof 42.44–43.95% with XMg [100 Mg/(Mg + Fe2+)] values varyingfrom 81 to 83. They show low CaO (<0.19%) and MnO (<0.08%)(Supplementary Table 1). The Mg# values, and the low concentra-tion in MnO and CaO for the olivine in this rock are similar to thoseof Alaskan-type intrusions (Snoke et al., 1981; Himmelberg andLoney, 1995; Johan, 2006).

5.1.2. ClinopyroxeneClinopyroxenes from the clinopyroxenite (sample XT24-2) are

characterized by high CaO content (24.16–25.02%), low Al2O3

(4.13–7.08%), TiO2 (0.36–0.76%), Na2O (0.05–0.10%), and narrow

variation in MgO (15.02–16.36%) and FeO (2.11–2.84%) withXMg[100 Mg/(Mg + Fe2+)] values ranging from 90 to 93(Supplementary Table 1). On the classification diagram for pyrox-ene (Lindsley, 1983), the compositional data are plotted in the fieldof diopside (Fig. 5a).

5.1.3. HornblendeThe hornblendes from hornblendite (sample XT24-1) are of parga-

sitic composition following the classification of scheme of Leake et al.(1997) (Fig. 5b), with relatively low SiO2 (36.84–39.26%), high Al2O3

(13.41–14.17%), and TiO2 (2.11–2.45%) and XMg[100 Mg/(Mg + Fe2+)]values in the range of 54–57 (Supplementary Table 1).

5.2. zircon morphology, trace elements and U–Pb geochronology

Zircon grains separate from one hornblendite and oneclinopyroxenite were analyzed using LA-ICP-MS method. Thesummary of the zircon U–Pb analytical results is presented inTable 2. Representative zircon CL images are displayed inFig. 6. The banded, patchy, and weak zoning together with theuniform internal texture of the zircon grains from these rockssuggest their high temperature origin (Corfu et al., 2003). Theage data are plotted in concordia diagrams in Fig. 7. The REEdata on zircon grains are listed in Table 3 and illustrated inFig. 8.

Fig. 3. Representative photographs showing field occurrences of the Longwangmiao intrusion. (a) The panoramic photo view of the exposed area of the intrusion from amining pit. (b) Hornblendite and clinopyroxenite exhibiting interlayering with sharp contact. (c) Fined grained hornblendite associated with calcite. (d) Medium to coarsegrained hornblendite showing preferred orientation of hornblende laths.


5.2.1. HornblenditeZircon grains separated from the hornblendite (XT24-1) are

transparent, colorless to light brown, prismatic or long elliptical.They show euhedral shapes with rounded terminations, and somegrains exhibit clear core-rim texture (Fig. 6a). The length of the zir-con grains range from 60 to 150 lm with aspect ratio of 3:1 to1.5:1. A total of 8 analyses were made on seven grains. Their Thcontents show a range of 27.3–355.1 ppm and U contents of20.8–994.2 ppm, with Th/U values of 0.30–1.31 (Table 2). On theconcordia diagram (Fig. 7a), the data form a well-defined interceptline with the concordia curve and yield upper intercept age of2509 ± 43 Ma and the lower intercept age of 378 ± 13 Ma. Threedata with young age are plotted close to the concordia line,and yield weighted 207Pb/206Pb mean age of 382 ± 10 Ma(MSWD = 0.56), very similar to the lower intercept age. The otherzircon grains with old ages exhibit 207Pb/206Pb age approximatelyclose to 2.5 Ga, indicating their inheritance from the Archean crus-tal basement. Their rare earth elements (REEs) normalized to chon-drite (Fig. 8a) exhibit obvious positive Ce anomalies and distinctiveheavy rare earth element (HREE) enrichment, further suggestingmagmatic origin (Griffin et al., 2002). The three zircon grains withyoung ages have elevated patterns compared to the old zircongrains and exhibit no Eu anomalies in contrast to the negative Euanomalies exhibited by the old zircon grains, suggesting that theyounger might have formed through remelting of the older ones.The conspicuous Pb loss of these zircon grains might correlate withthe younger magmatic event represented by the age of the newlyformed three zircon grains.

5.2.2. ClinopyroxeniteThe zircon grains separated from the clinopyroxenite (XT24-2)

are large in size with long axis ranging from 80 to 250 lm andaspect ratio of 2:1 to 1:1. These grains are transparent to translu-cent, and subhedral to anhedral with irregular shapes including

prismatic, elliptical and sub-rounded under CL images (Fig. 6b). Atotal of 22 spots were analyzed on 22 zircon grains. Except spot#1, 2, 4, 11, 18, 21 and spot #25 that fall under the concordia curvebecause of their high discordance(concordance is less than 85%),the other 15 analyzes are plotted on or close to the concordia curveand yield a weighted mean 207Pb/206Pb age of 399.1 ± 4.4 Ma(MSWD = 1.9) (Fig. 7b). Their Th, U and Th/U values are in the rangeof 1.0–58.2 ppm, 11.9–357.9 ppm, and 0.02–0.41 respectively(Table 2). The positive Ce anomalies and steep upward patternsfrom middle rare earth elements to heavy rare earth elements onchondrite normalized diagram (Fig. 8b) suggest their magmaticorigin. Thus, the weighted mean age is considered to representthe emplacement age of the clinopyroxenite.

5.3. Zircon Lu–Hf isotopes

Representative zircon grains were selected for in-situ Hf isotopeanalyzes after zircon U–Pb analyzes. A total of 14 spots were ana-lyzed on 14 grains from the two samples. The results are listed inTable 4 and illustrated in Fig. 9. The data show that most of the176Lu/177Hf ratios are less than 0.002, indicating the absence ofany major enrichment of radiogenic Hf after the formation of thezircons. Thus, the 176Hf/177Hf ratios can be used as a robust refer-ence to deduce the origin (Wu et al., 2007). The fLu/Hf values displaya tight range from �0.91 to �0.99, which are obviously lower thanthe fLu/Hf values of mafic crust (�0.34, Amelin et al., 2000) and sialiccrust (�0.72, Vervoort and Patchett, 1996). Wu et al. (2007) sug-gest that the two-stage model age is more precise than the singlestage model to evaluate the time of source material extractionfrom the depleted mantle or the residence time of the source mate-rial in the crust. The discrepancy of the two-stage model age andactual model age becomes larger when the ages of zircon are muchyounger. Four zircons from hornblendite analyzed for in-situ Hfisotopic composition (Table 4) can be divided into two groups in

Fig. 4. Representative photomicrographs under plane polarized light (a) and cross-polarized light (b–f) showing the petrographic characteristics of the various rock types inthis study. (a) Hornblende crystals in hornblendite. (b) Random distribution of hornblende crystals in fine grained hornblendite. (c) Coarse hornblende crystal withpoikiloblstic hornblende and apatite. (d) Clinopyroxene and magnetite in clinopyroxenite. (e) Olivine and clinopyroxene in clinopyroxenite. (f) Alteration of hornblenditeadjacent to calcite. Mineral abbreviations: Ol-olivine; Cpx-clinopyroxene; Hbl-hornblende; Ap-apatite; Cc-calcite; Mt-magnetite.

Table 1Summary of samples analyzed in this study with GPS reading and mineralogy.

Serial no. Sample no. Rock type GPS reading General mineralogy

1 OY-CD-1a Clinopyroxenite N41�13.3290 , E117�45.5720 Cpx + Ap + Mt + Py + Cc2 OY-CD-1c Hornblendite N41�13.5210 , E117�46.4120 Hbl + Mt + Ap3 OY-CD-1d Hornblendite N41�14.0270 , E117�45.9210 Hbl + Mt + Ap + Cc4 OY-CD-1f Clinopyroxenite N41�13.8290 , E117�46.3310 Cpx + Hbl + Mt + Cc + Py5 OY-CD-1k Hornblendite N41�13.5170 , E117�45.9220 Hbl + Cc + Ap + Mt + Py6 OY-CD-1l Hornblendite N41�13.5070 , E117�46.2340 Hbl + Mt + Ap + Cc7 OY-CD-1i Clinopyroxenite N41�13.6290 , E117�46.1380 Cpx + Ol + Py + Cc + Ap8 OY-CD-1j Clinopyroxenite N41�14.0270 , E117�46.2210 Cpx + Cc + Mt + Py9 XT24-1 Hornblendite N41�13.5330 , E117�46.4010 Hbl + Cc + Ap + Mt + Py

10 XT24-2 Clinopyroxenite N41�13.7380 , E117�46.4200 Cpx + Mt + Py + Ol + Cc11 XT29-2a Hornblendite N41�13.9080 , E117�45.7320 Hbl + Mt + Ap + Py + Cc12 XT29-4a Hornblendite N41�13.6620 , E117�45.8230 Hbl + Cc + Ap + Mt + Py

Mineral abbreviations: Cpx-clinopyroxene; Hbl-hornblende; Ol-olivine; Ap-apatite; Cc-calcite; Mt-magnetite; Py-pyrite.


terms of age. One zircon with the 207Pb/206Pb age of 2358.7 Mayielded 176Hf/177Hf value of 0.281452, eHf(t) value of 5.3, Hfdepleted mantle model ages (tDM) of 2487 Ma and Hf crustal modelages (tDM

C ) of 2566 Ma. In eHf(t) versus U–Pb age plot (Fig. 9), thisspot is close to the 2.5 Ga crust evolution line, suggesting thatthe source magma involved 2.5 Ga crust. The other three zircons

from the hornblendite exhibit 176Hf/177Hf ratio varying from0.282168 to 0.282204 and eHf(t) values ranging from �13.1 to�11.8 calculated with respect to the corresponding U–Pb age.Their Hf depleted mantle model ages(tDM) and Hf crustal modelages (tDM

C ) range from 1450–1527 Ma and 2123–2208 Ma respec-tively. Ten analyzes were carried out on ten zircon grains from

Table 2Zircon U–Pb analytical data for hornblendite and clinopyroxenite in this study.

Samplespots

Pb(ppm)

Th(ppm)

Uppm)

Th/U

207Pb/206Pbratio

1r 207Pb/235Uratio

1r 206Pb/238Uratio

1r 207Pb/206Pb(Ma)

1r 207Pb 5U(Ma)

1r 206Pb/238U(Ma)

1r Concordance

XT24-1-01 54.0 355.1 825.7 0.43 0.05523 0.00140 0.45614 0.01275 0.05990 0.00140 421.6 55.0 381 8.9 375.0 8.5 98XT24-1-02 349.3 294.9 994.2 0.30 0.15112 0.00321 6.46733 0.15859 0.31044 0.00724 2358.7 35.8 2041 21.6 1742.9 35.6 65XT24-1-04 78.3 50.7 171.6 0.30 0.16599 0.00358 9.11165 0.22700 0.39824 0.00936 2517.6 35.8 2349 22.8 2160.9 43.1 83XT24-1-05 83.1 209.6 159.7 1.31 0.15888 0.00369 8.05901 0.21228 0.36801 0.00877 2443.8 38.8 2237 23.8 2020.0 41.3 79XT24-1-06 43.2 56.9 162.2 0.35 0.05495 0.00120 0.47582 0.01198 0.06110 0.00158 410.2 46.7 395 7.8 382.3 9.7 97XT24-1-07 93.2 346.8 565.9 0.61 0.05569 0.00110 0.46843 0.01233 0.06194 0.00137 440.2 41.6 390 8.3 387.4 8.3 99XT24-1-08 12.3 27.3 20.8 1.31 0.16444 0.00463 9.37058 0.28905 0.41350 0.01034 2501.9 46.6 2375 28.3 2230.9 47.2 88XT24-1-09 132.4 205.2 276.2 0.74 0.16786 0.00381 8.65947 0.22687 0.38435 0.00898 2536.4 37.6 2302 23.9 2049.9 42.1 76XT24-2-01 6.1 15.2 86.8 0.18 0.06707 0.00247 0.59391 0.02191 0.06424 0.00091 839.8 74.7 473 14.0 401.4 5.5 82XT24-2-02 0.8 1.6 11.9 0.14 0.06577 0.01325 0.56905 0.11421 0.06276 0.00154 799.1 373.6 457 73.9 392.4 9.3 83XT24-2-03 2.1 1.9 31.2 0.06 0.05635 0.00526 0.49028 0.04556 0.06312 0.00109 465.3 195.1 405 31.0 394.6 6.6 97XT24-2-04 2.6 1.0 39.1 0.02 0.07017 0.00494 0.61795 0.04300 0.06388 0.00120 933.3 138.1 488 27.0 399.2 7.3 78XT24-2-06 5.5 22.0 80.1 0.28 0.05163 0.00262 0.45138 0.02286 0.06342 0.00094 268.9 112.1 378 16.0 396.4 5.7 95XT24-2-08 13.7 30.9 207.3 0.15 0.05639 0.00144 0.49001 0.01286 0.06302 0.00083 467.0 56.1 404 8.8 394.0 5.1 97XT24-2-09 4.2 9.0 63.8 0.14 0.05574 0.00339 0.48445 0.02933 0.06304 0.00100 441.7 130.1 401 20.1 394.1 6.1 98XT24-2-11 10.4 11.8 143.9 0.08 0.08359 0.00225 0.74542 0.02037 0.06468 0.00090 1282.8 51.7 565 11.9 404.0 5.5 60XT24-2-12 9.5 45.5 131.0 0.35 0.05473 0.00266 0.46909 0.02268 0.06216 0.00099 401.2 105.0 390 15.7 388.8 6.0 100XT24-2-13 3.1 8.4 45.6 0.18 0.05525 0.00418 0.48704 0.03672 0.06393 0.00107 422.4 160.8 402 25.1 399.5 6.5 99XT24-2-14 6.0 8.9 93.2 0.10 0.05187 0.00254 0.46106 0.02260 0.06446 0.00097 279.7 108.5 385 15.7 402.7 5.9 96XT24-2-15 7.1 23.3 105.5 0.22 0.05621 0.00231 0.48905 0.02015 0.06309 0.00091 460.0 89.3 404 13.7 394.4 5.5 97XT24-2-16 7.1 32.1 99.0 0.32 0.05746 0.00235 0.51218 0.02101 0.06464 0.00094 508.9 87.9 419 14.1 403.8 5.7 96XT24-2-17 14.5 49.6 206.0 0.24 0.05739 0.00218 0.48985 0.01861 0.06190 0.00091 506.1 81.7 404 12.7 387.2 5.5 95XT24-2-18 27.0 21.6 326.9 0.07 0.11508 0.00185 1.08185 0.01885 0.06818 0.00089 1881.1 28.7 744 9.2 425.2 5.4 25XT24-2-20 5.3 12.9 77.2 0.17 0.05557 0.00257 0.49600 0.02300 0.06473 0.00096 435.0 99.7 409 15.6 404.3 5.8 99XT24-2-21 10.9 58.2 140.8 0.41 0.08318 0.00434 0.70581 0.03627 0.06154 0.00112 1273.4 98.6 542 21.6 385.0 6.8 59XT24-2-23 8.1 44.7 113.6 0.39 0.05877 0.00206 0.51270 0.01810 0.06326 0.00090 558.7 74.5 420 12.2 395.4 5.5 94XT24-2-24 3.9 16.3 56.6 0.29 0.05095 0.00325 0.45498 0.02898 0.06475 0.00101 238.7 140.7 380 20.2 404.5 6.1 94XT24-2-25 2.9 2.1 40.4 0.05 0.08725 0.00475 0.78728 0.04253 0.06543 0.00112 1366.0 101.3 589 24.2 408.6 6.8 56XT24-2-26 24.0 49.3 357.9 0.14 0.05528 0.00107 0.49954 0.01032 0.06553 0.00086 423.3 42.2 411 7.0 409.2 5.2 99XT24-2-27 9.4 43.8 129.3 0.34 0.05925 0.00193 0.54443 0.01801 0.06664 0.00093 576.2 69.4 441 11.8 415.9 5.6 94

632X

.Tenget

al./Journalof

Asian

EarthSciences

113(2015)

626–643

/23

.6

.5

.3

.7

.2

.1

.0

.8

.4

.4

.1

.6

.2

.9

.1

.6

.6

.9

.0

.3

.9

.8

.5

.0

.3

.3

.8

.6

.4

.3

Fig. 5. Compositional diagrams showing the chemistry of representative minerals in hornblendite and clinopyroxenite. (a) Wollastonite–enstatite–ferrosilite diagramshowing compositions of orthopyroxene and clinopyroxene (Lindsley, 1983). (b) Classification diagram of hornblende in hornblendite from the Longwangmiao intrusion(after Leake et al., 1997).

Fig. 6. Representative cathodoluminescence (CL) images of zircons from hornblendite (XT24-1) and clinopyroxenite (XT24-2). The analytical spots for U–Pb (small yellowbroken circles) and Lu–Hf (large red broken circles) and age, initial eHf(t) values (in Ma) are also shown. (For interpretation of the references to color in this figure legend, thereader is referred to the web version of this article.)

Fig. 7. Zircon U–Pb concordia plots and weighted mean 206Pb/238U age (inserted figures) for hornblendite (a) and clinopyroxenite (b) from the Longwangmiao intrusion.


Table 3REE abundances(ppm) in zircongrains from the hornblendite(a) and clinopyroxenite(b) in the Longwangmiao intrusion.

Element La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

XT24-1XT24-1-01 <0.049 8.07 0.14 3.2 16.59 15.37 143.43 50.95 595.88 203.08 725.17 117.3 841.95 112.31XT24-1-02 0.22 16.37 <0.112 0.44 0.96 <0.214 7.31 3.05 41.56 19.5 104.93 26.16 298.66 69.89XT24-1-04 <0.048 20.38 <0.055 0.67 1.25 0.37 6.79 2.48 30.83 12.38 60.96 14.2 150.96 32.85XT24-1-05 <0.144 41.59 <0.125 1.61 4.19 1.17 18.07 5.56 62.68 23.09 104.29 22.88 232.61 48.99XT24-1-06 0.79 12.45 0.99 4.57 12.34 21.22 200.24 78.29 860.24 258.93 981.32 169.21 1351.43 220.21XT24-1-07 1.31 15.43 1.12 2.98 14.22 17.53 136.78 41.24 496.23 177.64 632.87 128.44 947.78 145.28XT24-1-08 4.1 35.03 1.57 10.4 6.1 1.35 16.86 5.32 56.56 20.22 86.93 18.17 174.24 34.16XT24-1-09 1.99 49.1 0.61 3.73 4.38 1.8 18.65 6.03 65 23.86 104.66 22.04 223.58 45.19

XT24-2XT24-2-01 0.0262 1.897 <0.0240 0.178 0.428 0.259 2.47 0.89 11.15 5.14 26.53 6.33 73.16 18.05XT24-2-02 <0.0202 0.532 0.025 0.065 <0.14 0.216 1.121 0.536 7.43 3.6 21.54 5.87 78.1 22.99XT24-2-03 0.0306 0.812 0.0352 <0.046 <0.136 0.46 2.51 0.927 15.69 8.14 47.89 13.05 169.4 49.93XT24-2-04 <0.0174 0.613 <0.0208 0.065 0.579 0.736 5.48 2.702 44.11 24.33 143.93 37.6 491 151.23XT24-2-06 <0.0206 2.94 <0.0236 0.366 0.533 0.382 3 0.876 10.73 4.77 26.57 6.89 80.17 20.24XT24-2-08 <0.0188 2.037 <0.0237 0.168 0.233 0.334 1.795 0.706 10.6 5.28 31.01 8.1 106.24 33.59XT24-2-09 <0.0205 3.26 <0.0220 0.804 1.701 2.312 13.29 5.18 65.7 30.31 159.6 38.4 461.49 127.91XT24-2-11 <0.0168 3.95 <0.0211 0.482 0.696 0.913 5.33 2.044 28.64 14.07 78.2 20.13 248.46 71.09XT24-2-12 0.0169 3.02 0.0559 0.167 0.322 0.251 1.77 0.568 7.12 3.09 15.88 3.85 43.74 10.6XT24-2-13 <0.0182 1.706 <0.0231 0.112 0.289 0.209 1.844 0.605 7.8 3.46 17.68 4.23 50.88 13.03XT24-2-14 <0.0153 2.414 0.0364 <0.070 <0.171 0.702 5.67 2.43 37.11 17.92 100.39 25.41 311.19 87.52XT24-2-15 0.0166 2.207 <0.0244 <0.061 <0.154 0.057 1.26 0.516 6.46 3.19 17.85 4.69 56.31 15.35XT24-2-16 <0.0168 2.171 <0.0200 0.09 0.215 0.162 0.934 0.35 4.76 2.3 12.33 3.25 39.62 10.69XT24-2-17 <0.0177 10.05 0.068 1.077 2.74 3.78 24.92 9.03 126.83 60.12 312.94 72.75 846.55 241.47XT24-2-18 <0.0181 1.87 0.0274 0.374 2.82 3.67 28.69 12.9 178.46 79.02 394.22 89.71 947.27 213.23XT24-2-20 <0.0183 3.7 <0.0206 0.303 0.802 1.135 8.13 3.54 54.85 28.25 162.08 40.95 510.91 154.29XT24-2-21 <0.0181 4.94 0.0498 0.586 0.952 0.973 6.55 2.273 28.68 12.7 63.43 14.81 159.97 37.13XT24-2-23 <0.0166 3.47 <0.0190 0.175 0.436 0.413 2.69 0.981 13.43 6.7 36.88 9.35 116.6 33.29XT24-2-24 <0.0194 2.446 <0.0232 0.107 <0.137 0.158 1.38 0.506 6.75 3.11 16.41 4 47.52 11.66XT24-2-25 <0.0205 1.42 <0.031 0.081 0.154 0.105 <0.121 0.146 1.581 0.747 4.22 1.164 13.54 3.78XT24-2-26 <0.0185 6.49 0.0388 1.715 5.04 4.76 33.76 10.43 121.68 46.9 212.6 45.59 467.38 106.62XT24-2-27 0.0232 2.95 0.035 0.316 0.581 0.299 3 0.952 12.63 5.46 29.44 7.01 82.9 19.95

Fig. 8. Chondrite-normalized REE patterns for zircons from the hornblendite (a) and clinopyroxenite (b).


the clinopyroxenite, and the results show 176Hf/177Hf ratios in therange of 0.282102–0.282248. They show limited variation in eHf(t)values from �14.9 to �10.0. The Hf depleted mantle model ages(tDM) of these zircons range from 1388 Ma to 1600 Ma and the Hfcrustal model ages (tDM

C ) of 2021–2341 Ma with the U–Pb ages of388.8–404.5 Ma. Their plots in Fig. 9 are similar to theyoung-aged group zircon from hornblendite and their upwarddeviation trend from the 2.5–3.0 crust evolution line may indicatethe additional input of mantle materials.

5.4. Whole rock geochemical characteristics

The least altered and homogeneous portions of 12 samples werecrushed and powdered to 200 mesh for geochemical analyses afterpetrographic observation, in order to select samples in which

primary igneous textures and minerals are preserved. The LOI(<6 wt.%) and the lack of its correlation with mobile elements, suchas K, Na, Ca, Rb, suggest that the possible alteration in these sam-ples are negligible. This inference is further substantiated by theirCe anomalies which show a restricted range of 0.9–1.1(Supplementary Table 2), as well as the high degree of other ele-mental correlation with the least mobile Zr on binary diagramswith coefficient (R) >0.75 (figure not shown).

Both the hornblendite and clinopyroxenite samples have lowSiO2 content, with the hornblendite samples exhibiting relativelow SiO2 content varying from 31.52 wt.% to 37.44 wt.%. TheSiO2 content in the clinopyroxenite samples range from 35.91 to40.59 wt.%. In terms of Mg# [100 �Mg/(Mg + Fe2+); FeO =Fe2O3/1.15], the hornblendite samples fall in the high Mg# group(42.40–52.44) with high contents of Fe2O3

T(17.91–23.70 wt.%)

Table 4LA-MC-ICPMS Lu-Hf isotope data on zircons from hornblendite and clinopyroxenite.

No. Age (Ma) 176Yb/177Hf 176Lu/177Hf 176Hf/177Hf 1s 176Hf/177Hfi Epsilon Hf(0) Epsilon Hf(t) TDM (Ma) TDMC (Ma) fLu/Hf

XT24-1 HornblenditeXT24-1-01 375 0.006400 0.001332 0.282179 0.000016 0.282170 �21.0 �13.1 1527 2200 �0.96XT24-1-02 2358.7 0.013895 0.000523 0.281452 0.000022 0.281428 �46.7 5.3 2487 2566 �0.98XT24-1-06 382.3 0.006344 0.000242 0.282204 0.000014 0.282202 �20.1 �11.8 1450 2123 �0.99XT24-1-07 387.4 0.020880 0.000741 0.282168 0.000014 0.282163 �21.4 �13.0 1519 2208 �0.98

XT24-2 ClinopyroxeniteXT24-2-03 394.6 0.051067 0.002847 0.282220 0.000014 0.282199 �19.5 �11.6 1531 2122 �0.91XT24-2-06 396.4 0.003134 0.000173 0.282186 0.000012 0.282185 �20.7 �12.1 1472 2154 �0.99XT24-2-08 394 0.003257 0.000183 0.282160 0.000012 0.282159 �21.6 �13.0 1508 2213 �0.99XT24-2-09 394.1 0.028867 0.001497 0.282213 0.000014 0.282202 �19.8 �11.5 1486 2116 �0.95XT24-2-12 388.8 0.004511 0.000202 0.282248 0.000014 0.282247 �18.5 �10.0 1388 2021 �0.99XT24-2-13 399.5 0.004629 0.000214 0.282109 0.000014 0.282107 �23.4 �14.7 1579 2324 �0.99XT24-2-14 402.7 0.019594 0.001045 0.282203 0.000014 0.282195 �20.1 �11.6 1482 2126 �0.97XT24-2-15 394.4 0.005412 0.000271 0.282177 0.000012 0.282175 �21.0 �12.5 1488 2176 �0.99XT24-2-16 403.8 0.009047 0.000515 0.282201 0.000012 0.282197 �20.2 �11.5 1464 2121 �0.98XT24-2-24 404.5 0.011622 0.000494 0.282102 0.000016 0.282098 �23.7 �14.9 1600 2341 �0.99

Note: 176Lu decay constant k = 1.867 � 10�11 yr�1 (Söderlund et al., 2004); Chondritic values: (176Lu/177Hf)CHUR = 0.0332 ± 0.0002, (176Hf/177Hf)CHUR = 0.282772 ± 0.000029(BlichertToft and Albarede, 1997); depleted mantle values: (176Lu/177Hf)DM = 0.0384, (176Hf/177Hf)DM = 0.28325 (Griffin et al., 2000); Hfi: initial Hf isotope compositionfor U–Pb age; fLu/Hf = (176Lu/177Hf)sample/(176Lu/177Hf)CHUR � 1; TDM = 1/k � ln{1 + [(176Hf/177Hf)sample � (176Hf/177Hf)DM]/[(176Lu/177Hf)sample � (176Lu/177Hf)DM]}; TDM

C =1/k � ln{1 + [(176Hf/177Hf)sample,t � (176Hf/177Hf)DM,t]/[(176Lu/177Hf)c � (176Lu/177Hf)DM]} + t; (176Lu/177Hf)c = 0.015; t = crystallization time of zircon. The 176Hf/177Hf ratiosreported were corrected according to the recommended value of the standard zircon 91500.

Fig. 9. Plot of eHf(t) versus U–Pb Age from Early Ordovician to Early Cretaceous magmatic bodies in the northern Hebei and kimberlites in eastern North China Craton. Hfisotopic compositions of zircons from dacite and rhyolite are from Yang et al. (2006b). Hf isotopic compositions of zircons from Neoarchean granitoid gneisses are from Liuet al. (2011). Hf isotopic compositions of zircons from Xianghuangqi hornblende gabbro, Wudaoyingzi diorite, Tianqiao quartz diorite, Lingying granodiorite, Zhoutaizi quartzdiorite are from Zhang et al. (2009a). Hf isotopic compositions of zircons from Hongshila pyroxenite, Xiahabaqin rodingite, Baiqi hornblendite and Boluonuo hornblendegabbro are from Zhang et al. (2009b). Hf isotopic compositions of zircons from Kimberlites in eastern North China Craton are from Zhang and Yang (2007). Hf isotopiccompositions of zircons from Xiaozhangjiakou mafic–ultramafic complex are from Tian et al. (2007). The Hf isotopic value of enriched mantle of North China Craton is fromChen et al. (2008) and Yang et al. (2006a). (For interpretation of color in Figure, the reader is referred to the web version of this article.)


and TiO2 (1.78–2.73 wt.%), whereas the clinopyroxenite samplesfall in the low Mg# group (�33.80–42.04) with high contents ofFe2O3

T (8.32–16.82 wt.%) and TiO2 (0.64–1.64 wt.%). These featuresprobably suggest metasomatism of calcium-rich fluids during ser-pentinization of the ultramafic rocks (Attoh et al., 2006). The horn-blendites and clinopyroxenites display high CaO contents from13.10 wt.% to 19.47 wt.%, corresponding to their high contents ofclinopyroxene, hornblende, apatite and the presences of some sec-ondary calcite related to the later hydrothermal fluid influx afterthe main crystallization event. The sub-alkaline nature of theLongwangmiao intrusion is suggested by plots in the field ofsub-alkaline basalt on the Zr/TiO2 versus Nb/Y diagram

(Winchester and Floyd, 1976) (Fig. 10a). The broadly tholeiiticaffinities of the intrusion is further corroborated by the distribu-tion in the ternary FeOtotal � Na2O + K2O �MgO diagram (Kuno,1968; Irvine and Baragar, 1971) and ternary TiO2 � 100 � Y + Zr–Cr diagram (Davies et al., 1979) (Fig. 10b and c).

The hornblendites and clinopyroxenites show similar patternson the chondrite-normalized REE diagram (Fig. 11a) with negligi-ble or slight positive Eu anomalies (�1.00–1.43) and convex pat-terns with peaks at Pr–Nd, which is typical for clinopyroxene andhornblende megacrysts precipitated from, and equilibrated with,light-REE enriched basaltic melts (Irving and Frey, 1984). The rocksexhibit moderate light REE enrichment with (La/Yb)N ratios

Fig. 10. (a) Zr/TiO2 versus Nb/Y classification diagram for whole-rock samples(after Winchester and Floyd, 1976). (b) Ternary plot ofFeOtotal � Na2O + K2O �MgO. The black curve is from Kuno (1968) and the redone is from Irvine and Baragar (1971). (c) Ternary TiO2 ⁄ 100 � Y + Zr � Cr diagram(Davies et al., 1979).


ranging from 4.37 to 10.22. The depletion of La and Ce relative to Prand Nd also indicates that the whole rock geochemistry is con-strained by the mineralogical compositions of cumulate horn-blende and clinopyroxene, which is a typical feature resultingfrom clinopyroxene/liquid and hornblende/liquid partition coeffi-cients (Schnetzler and Philpotts, 1970).

Rocks from the Longwangmiao intrusion normally display highcontents of Sr (hornblendite: 392–679 ppm, clinopyroxenite:1837–2437 ppm) and Ba (hornblendite: 149–307 ppm, clinopyrox-enite: 195–572 ppm). The Sc, V, Cr, Co, Ni, Cu and Zn contents arealso relatively high, which correspond to the presence of magnetiteand sulfides, including sphalerite, chalcopyrite and chalcocite. Inthe primitive mantle-normalized variation diagram (Fig. 11b), thehornblendites show positive Ba, K, P, anomalies and negative Th,U, Nb, Ta, Zr and Hf anomalies. The clinopyroxenites display almostparalleled but descending pattern as compared to hornblenditeswith positive peak at Ba, K and Sr and same nadir at Th, U, Nb,Ta, Zr and Hf.

Fig. 11. (a) Chondrite-normalized REE patterns for hornblendite and clinopyroxenclinopyroxenite. Both chondrite values and primitive mantle values are from Sun and M

Both rock types exhibit some systematic variation of selectedmajor oxides and trace elements against Mg# (Figs. 12 and 13),indicating fractional crystallization. In general, the TiO2 andFe2O3 values show positive correlation with the decrease of Mg#(Fig. 12a and c), whereas the Al2O3 values show negative correla-tion with the decrease of Mg# (Fig. 12b). The CaO values are gen-erally constant (Fig. 12d), whereas Na2O and K2O values exhibitscattered distribution (Fig. 12e and f). The Mg#, Ni and Nd decreasefrom hornblendite to clinopyroxenite (Fig. 13a and d), accompa-nied by asystematic increase in Al2O3 and incompatible Sr(Fig. 13c), correlating with the increasing modal content ofclinopyroxene from hornblendite to clinopyroxenite. The positivecorrelation of TiO2, Fe2O3

T, Cr, and V versus increasing Mg#(Figs. 12a, c and 13b, e) indicates the increasing modal magnetiteand metal sulfides in hornblendite. The constant relationshipbetween CaO and Mg# may correspond to the diopsidic contentfor clinopyroxene and pargasitic content for hornblende (Fig. 5),which are both important reservoirs for calcium. Barium exhibitsirregular variation versus Mg# (Fig. 13f), together with the scat-tered correlation of Na2O and K2O versus Mg#, suggesting littleplagioclase in these rocks, which is also supported by their slightEu anomalies (Fig. 11a and Supplementary Table 2).

6. Discussion

6.1. Crystallization age of the Longwangmiao intrusion

Mafic–ultramafic intrusions are widely distributed in the north-ern margin of the NCC (Tian et al., 2007; Zhang et al., 2009a,b; Zhaoet al., 2007), with emplacement ages ranging from MiddleDevonian to Triassic. In this study, the zircon LA-ICP-MS U–Pbgeochronology of the clinopyroxenite has yielded a reliable crystal-lization age for the Longwangmiao intrusion as 399.1 ± 4.4 Ma. Thezircon analytical data from the hornblendite define an upper inter-cept age of 2509 ± 43 Ma and a lower intercept age of 378 ± 13 Ma.The lower intercept age is almost identical to the weighted207Pb/206Pb mean age of 382 ± 10 Ma of three concordant zircongrains. This age is slightly younger than the emplacement of theclinopyroxenite and might correspond to the late hydrothermalstage. Among the ultramafic–mafic intrusions in the regionreported in previous studies, the Hongshilapyroxenite–hornblendite complex and the Erdaogou–Xiahabaqinpyroxenite–hornblendite–rodingite complex exhibit crystallization ages around395 Ma and hydrothermal age around 380 Ma (Zhang et al.,2009b), similar to the ages reported in our study. These data sug-gest that the Longwangmiao intrusion may share similar tectonicsetting with the other Devonian mafic–ultramafic intrusions inthe northern NCC.

ite. (b) Primitive mantle-normalized variation diagrams for hornblendite andcDonough (1989). The shade areas are from Zhang et al. (2009b).

Fig. 12. Co-variation diagrams showing Mg# versus TiO2 (a), Al2O3 (b), Fe2O3T (c), CaO (d), Na2O (e), K2O (f).


6.2. Petrogenetic implications

Given the close field relationship between the hornblendite andclinopyroxenite, together with their broadly comparable U–Pb ages(Fig. 7) as well as similar Hf isotopic compositions (Table 4 andFig. 9), these two lithologies are considered to have originated fromthe same magma source. This inference is further corroborated bytheir chondrite-normalized REE patterns and primitivemantle-normalized trace elements patterns (Fig. 11a and b), aswell the correlations of the different oxides and trace elements ver-sus Mg# (Figs. 12 and 13).

Most immobile elements, such as Zr, Nb, Ta, V, Cr and REEs,display good correlations with the silica contents, which areconsistent with their relatively incompatible behavior duringmagmatic process. These rocks exhibit Ce/Yb and P2O5/Al2O3

ratios in the range of 1.29–2.65, and 0.02–0.35, respectively,and indicate low degree of melting from the source region(Green et al., 1974; Langmuir et al., 1992; Furman, 1995). Therelative abundances of La, DY, Sm, Tb and Yb are stronglydependent on the degree of partial melting and the nature ofthe aluminous phase – spinel or garnet – in the mantle source(Thirlwall et al., 1994; Furman, 1995; Kinzler, 1997; VanWestrenen et al., 2001; Bogaard and Wörner, 2003). Thus, these

element ratios provide an effective method to evaluate thedepth of melting. The near constant Dy/Yb (3.01–4.06) andLa/Yb (6.09–14.25) values of these rocks suggest garnet facies(Fig. 14a), indicating partial melting of a relatively deepgarnet-bearing source (Thirlwall et al., 1994; Bogaard andWörner, 2003; Jung et al., 2006).

The Longwangmiao ultramafic intrusion is characterized by theoccurrence of clinopyroxene and hornblende-rich assemblages inthe absence of orthopyroxene and plagioclase-rich assemblages,together with the cumulate nature (Fig. 4b) and differentiationtrends (Figs. 12 and 13). These features suggest that theLongwangmiao intrusion is in some respects similar withAlaskan-type intrusions (Irvine, 1974; Helmy and El Mahallawi,2003; Eyuboglu et al., 2010; Ishiwatari and Ichiyama, 2004;Snokeet al., 1981; Himmelberg and Loney, 1995; Batanova et al., 2005;Johan, 2006; Deng et al., 2013). The parental magma forAlaskan-type intrusions is considered to be of picritic composition(Irvine, 1974; Tistl et al., 1994; Helmy and El Mahallawi, 2003).According to our mineralogical studies, the major minerals (oli-vine, clinopyroxene and hornblende) exhibit high Mg# values inboth rock types. Based on the Mg# of the olivine (81–83) andFe–Mg partitioning between olivine and liquid (Fe/Mgol-liqKD = 0.3; Roeder and Emslie, 1970), the Mg# of the primitive

Fig. 13. Co-variation diagrams showing Mg# versus selected trace elements as follows: Ni (a), Cr (b), Sr (c), Nd (d), V (e), Ba (f).

Fig. 14. Representative trace and rare earth element ratio diagrams illustrating the petrogenetic characteristics of the Longwangmiao intrusion. (a) Dy/Yb versus La/Yb plot;(b) La/Ba versus La/Nb plot. The general trends for melting in the spinel- and garnet-peridotite facies in (a) are from Jung et al. (2006). The field in (b) is from Saunders et al.(1992).


parental magma can be calculated as 56–59. As discussed above,the magma from which the two lithologies evolved were generatedthrough low degree partial melting of garnet-bearing peridotitefacies. The Mg# of the parental magma could also be estimated

as ca. 54 from the node between two differentiation curves inthe variation diagrams (Fig. 12a–c). These features confirm thatthe parental magma was high magnesian, with affinity to parentalpicritic composition.


The common presence and abundance of hornblende in theLongwangmiao rocks suggests that the parental magma washydrous, which is further substantiated by the high Wo andCr2O3 contents of clinopyroxene and high Fo and NiO contents ofolivine, which are near-liquidus crystallization products ofwater-bearing magmas (Sisson and Grove, 1993). Thus, the earlycrystallized phase could be water-bearing hornblende, and the fol-lowing the consumption of the water, the water-poor phase crys-tallized the clinopyroxene and olivineat the later stage, similar tothe features in other Alaskan-type intrusions (Helmy and ElMahallawi, 2003).

Several scenarios have been proposed for petrogenesis of cumu-lated pyroxenite. These include primary magma partially meltedfrom peridotite facies at lithospheric mantle or asthenosphericmantle (Irving, 1980; Suen and Frey, 1987), products resulted bythe reaction between mantle peridotite and silica-enriched meltsreleased by conducted slab (Kelemen, 1995; Kelemen et al.,1998), and residual melt after re-partial melting of the previousformed mantle-derived magma (Frey and Prinz, 1978). In thisstudy, although some inherited zircon grains of Archean age arepresent, the broadly identical Lu–Hf isotopic compositions of theDevonian zircons and the limited variation of zircon eHf(t) valuesindicate that there was no significant crustal contamination duringthe ascent of the parental magma (Fig. 9). The eHf(t) values ofDevonian ages are in the range of �13.1 to �11.8 for the horn-blendite and �14.9 to �10.0 for the clinopyroxenite. The negativeeHf(t) values indicate that the parental magma was derived from anenriched source, thus, the possibility of depleted mantle origin canbe precluded. Both enriched mantle and/or reworked crust canyield the negative eHf(t) values obtained in this study. In the epsi-lon Hf versus U–Pb age (Ma) diagram (Fig. 9), the isotopic data plotbetween the array defined by the evolution line of 2.5–3.0 Ga Neo-to Mesoarchean basement rocks in the NCC and the presumedsub-continental lithospheric mantle area (the yellow shade inFig. 9), suggesting that the source of the magma is entirely linkedto the reworked crustal material but also show affinity to thesub-continental lithospheric mantle. We envisage the possible ori-gin of the parental magma at the mantle-crust boundary, with thecrustal signature resulting from subduction-related components,which is common for most Alaskan-type intrusions as proposedby Taylor (1967) and Irvine (1974). The above features favor thesecond scenario for the cumulate petrogenesis of clinopyroxenite.The complete reaction of mantle peridotite component and crustalmaterials led the magma becoming homogeneous and moreenriched in silica. At the same time, the input of silica transformedthe original magma to evolve into basaltic composition.

The ratios between highly incompatible trace elements can beutilized to deduce mantle source region characteristics, even formoderately evolved magmas. The ratios of La, Ba and Nb, whichshow only limited change under various petrogenetic processessuch as partial melting or fractional crystallization, are widely usedas tracers to differentiate between the contribution of convectingand non-convecting part of the mantle to the sources of basalticrocks (Saunders et al., 1992; Peate, 1997; Jourdan et al., 2007). Inthe La/Ba versus La/Nb plot (Fig. 14b), all our samples are plottedin the field different from that for typical oceanic island basaltsand mid oceanic riftbasalt, precluding the asthenospheric mantleas the source (Saunders et al., 1992), and suggesting lithosphericaffinity. This inference is also corroborated by Nb/U and Ce/Pbratios of the hornblendite and clinopyroxenite samples, whichare in the range of 1.90–23.11 and 2.89–20.35, respectively, show-ing marked difference from those of MORB and OIB (Nb/U � 47 andCe/Pb � 25; Hofmann, 1988).

Experimental studies of Green et al. (2004) show that par-tialmelting of refractory lherzolitic mantle fluxed by H2O + CO2

can give rise to hydrous, island-arc picritic ankaramite magmas.

In this study, the arc magma affinity of the intrusionis also sup-ported by the enrichment in LILEs (e.g., Rb, K, Ba, Pb, and Sr) andLREEs, but conspicuous depletion of HFSEs (Nb, Zr, Ti) in thechondrite-normalized REE patterns and primitivemantle-normalized trace element spidergrams (Fig. 11a and b).These chemical features largely owe to element fluxes derivedfrom the subducting oceanic lithosphere (Hawkesworth andEllam, 1989; McCulloch and Gamble, 1991; Saunders et al., 1991).

In summary, we propose that the initial bath of magma washigh magnesian and island-arc picritic in composition derived bylow degree partial melting of garnet-bearing peridotite facies froman enriched sub-continental lithospheric mantle. The magma sub-sequently evolved into basaltic composition through the input ofsilica-rich crustal materials in a subduction setting. The magmabecame hydrous through fluids derived from the subducted slab.

6.3. Comparison with other contemporary intrusions

Extensive felsic and mafic magmatic rocks were emplaced alongthe northern margin of the NCC during late Paleozoic to earlyMesozoic (Pan, 1996; Zhang et al., 2007a,b). These intrusions pro-vide important constraints on the isotopic and geochemical char-acteristics of the sub-continent lithospheric mantle beneath theNCC prior to prior to the onset of the lithosphere destruction andthinning in Late Mesozoic.

Although these magmatic bodies exhibit different rock assem-blages, field occurrences and emplacement age, they all broadlycorrespond to Andean-type continental arc magmas (Zhang et al.,2007a,b, 2009a). Among these plutons, intrusions which exhibitemplacement age similar to that of the Longwangmiao intrusionsmay share a common tectonic setting. Previous studies onthese Devonian plutons show ages in the range of 397–364 Ma,including the Shuiquanguanquartz monzonite and syenite,Gushanmonzodiorite, Erdaogou amphibolite, Xiahabaqinrodingite,Hongshilapyroxenite, Chehugousyenite porphyry, and the rhyoliteand K-feldspar granite from Chifeng area (Luo et al., 2001; Ni,2002; Zhang et al., 2007a, 2009b; Liu et al., 2010; Shi et al.,2010; Ye et al., 2014). The felsic magmatic bodies are metalumi-nous and calc-alkaline, with nil or slight positive Eu anomalies(Jiang, 2005; Zhang et al., 2007a, 2009b; Wan et al., 2009). TheSr–Nd isotopic and zircon Hf isotopic data suggest that some ofthese felsic bodies were derived from magmas that involved themelted components of ancient lower crust (e.g., Chehugousyeniteporphyry; Wan et al., 2009) whereas some others were derivedfrom the partial melting of enriched lithospheric mantle with inputof crustal materials (e.g., Shuiquangou alkaline complex andGushanmonzodiorite; Jiang, 2005; Zhang et al., 2007a). Amongthese Devonian plutons, the Hongshila pyroxenite-hornblenditecomplex and Erdaogou–Xiahabaqin pyroxenite–hornblendite–rodingite complex show rock assemblages similar to theLongwangmiao intrusion. Zhang et al. (2009b) reported whole rockneodymium isotopic values from the Hongshila andErdaogou-Xiahabaqin complexes which show relatively low initial87Sr/86Sr values from 0.70467 to 0.70706, epsilon Nd(t) rangingfrom �15.5 to �1.5, and zircon epsilon Hf(t) varying from �6.5to 5.5, indicating origin by partial melting of slightly enrichedlithospheric mantle with incorporation of different proportion ofcrustal materials. As discussed above, the Longwangmiao intrusionalso shows an enriched sub-continental lithospheric mantle sourcewith involvement of crustal materials. In Fig. 9, the shaded arraymay indicate the evolution of the SCLM beneath the North ChinaCraton from early Paleozoic to Middle Mesozoic by consideringthe Hf isotopic value of the �490 Ma mantle zircons fromXiaozhangjiakou mafic–ultramafic intrusion (Tian et al., 2007).The blue line and continuous black broken line represent the aver-age epsilon Hf(t) values for SCLM. Compared to the Hongshila

Fig. 15. Nb/Zr versus Zr (ppm) discriminated plot (a) from Thieblemont and Tegyey (1994) and Log-transformed immobile trace element tectonic discrimination diagrams (b,c) from Agrawal et al. (2008) for Longwangmiao intrusion, Hongshila complex and Erdaogou-Xiahabaqin complex. For IAB-CRB-OIB-MORB diagram, DF1 = 0.3518 ⁄ Log(La/Th) + 0.6013 ⁄ Log(Sm/Th) � 1.3450 ⁄ Log(Yb/Th) + 2.1056 ⁄ Log(Nb/Th) � 5.4763 and DF2 = �0.3050 ⁄ Log(La/Th) � 1.1801 ⁄ Log(Sm/Th) + 1.6189 ⁄ Log(Yb/Th) + 1.2260 ⁄Log(Nb/Th) � 0.9944. For IAB-CRB-MORB diagram, DF1 = 0.3305 ⁄ Log(La/Th) + 0.3484 ⁄ Log(Sm/Th) � 0.9562 ⁄ Log(Yb/Th) + 2.0777 ⁄ Log(Nb/Th) � 4.5628 andDF2 = �0.1928 ⁄ Log(La/Th) � 1.1989 ⁄ Log(Sm/Th) + 1.7531 ⁄ Log(Yb/Th) + 0.6607 ⁄ Log(Nb/Th) � 0.4384. IAB-island-arc basic rocks, CRB-continental-rift basic rocks, OIB-ocean-island basic rocks, MORB-mid-oceanic ridge basic rocks.


complex and Erdaogou-Xiahabaqin complex, the Longwangmiaointrusion exhibit more negative epsilon Hf values, indicating therelatively higher involvement of crustal materials than the formertwo. In the chondrite-normalized REE patterns and primitivemantle-normalized spider diagrams (Fig. 11a and b), all the threecomplexes share similar patterns but the rock samples fromLongwangmiao intrusion exhibit a descending trend compared tothose from the other two complexes. In the Dy/Yb versus La/Ybplot and La/Ba versus La/Nb plot (Fig. 14a and b), they are broadlydistributed in the same region. All these features converge to indi-cate ananalogous setting for magma genesis. The differences inplots in Figs. 11 and 14 largely reflect the relatively different pro-portion of the crustal components.

6.4. Tectonic setting and an integrated petrogenetic model

Arc accretion widely occurred along the northern margin of theNCC during Paleozoic as evidenced from the zircon U–Pb age vary-ing from 490 to 446 Ma reported from accretionary units associ-ated with the active southward subduction of Mongolian oceanicslab beneath the NCC (Xiao et al., 2003; Windley et al., 2007).The subduction continued through mid-to late Mesozoic, as sug-gested by the occurrence of the Andean-type continental arc mag-matism on the northern margin of the NCC (396–270 Ma; Zhanget al. 2007a,b, 2009a–c; Zhang and Zhao, 2013). The subductionceased probably in late Permian and was accompanied by the finalcollision between the NCC and the Mongolian micro-continentsalong the Solonker suture (Chen et al., 2000, 2009a; Xiao et al.

2003), as suggested by the occurrence of the abundant granitoidsthat intruded into the Solonker suture zone (Chen et al., 2000,2009a). Most studies have proposed that that these LateCarboniferous to Early Permian plutons are closely related to thewaning stage of the oceanic subduction beneath the NCC and fol-lowing arc-related compression to back-arc extension after thefinal collision of between NCC and the Mongoliamicro-continents (Chen et al., 2009a,b). The Longwangmiao intru-sion of this study together with the Hongshila andErdaogou-Xiahabaqin complexes show Devonian emplacementages, with formation in subduction-related setting (Fig. 15a)(Thieblemont and Tegyey, 1994), correlating with the convergenceof the Mongolian oceanic slab. In the log-transformed immobiletrace element tectonic discrimination diagrams proposed byAgrawal et al. (2008), these rock samples fall in the area of IAB areato CRB + OIB area (Fig. 15b), whereas in the IAB-CRB-MORB dia-gram (Fig. 15c), they plot in the area of IAB to CRB. These featuressuggest a post collisional extensional setting for theLongwangmiao intrusion, which is further supported by theirtholeiitic nature (Fig. 10b and c). However, the emplacement tim-ing during Devonian marks the early subduction stage of the ocea-nic slab beneath the NCC as discussed above. The accretionary beltsalong the northern margin of the NCC are composed of a series ofmicro-terranes. They amalgamated to the NCC successively beforethe final collision between the Siberian Block and NCC. Amongthese mirco-terranes, the Bainaimiao terrane is typically character-ized by volcanic rock assemblages including basalt, andesite andrhyolite. These rocks exhibit calc alkali island arc nature, and


therefore the Bainaimiao terrane is considered as an arc (Zhang,2013). The formation age of the Bainaimiao arc is constrainedwithin the range from �475 Ma (Early Ordovician) to �420 Ma(Late Silurian) based on U–Pb ages (Liu et al., 2003; Jian et al.,2008; Zhang and Jian, 2008). The final collision for theBainaimiao arc and the NCC occurred at the waning stage ofSilurian (Li et al., 2009). The magmatic activities during Devonianwere linked to the post-collisional extension between the conti-nent and the arc (Hu et al., 1990; Tang and Yan, 1993) where anisland arc amalgamated to the northern NCC in the latest EarlyPaleozoic after, and a continental arc developed along the northernmargin of the NCC (Xiao et al., 2003). The slightly enriched signa-ture of the SCLM inferred from the Middle Devonian mafic–ultra-mafic rocks suggests that the lithosphere and continental marginof the northern NCC were not strongly influenced by thePaleo-Asian tectonic system during the Early Paleozoic to MiddleDevonian. In summary, the Middle Devonian felsic and mafic–ul-tramafic rocks were likely emplaced in a post-collisional exten-sional environment after arc-continental collision between theBainaimiao arc and the northern NCC during the Late Silurian.

7. Conclusion

(1) The Longwangmiao intrusion was emplaced at ca. 399 Ma.The Middle Devonian magmatism marks the earliest amongthe three main pulses of magmatism (Middle Devonian, LateCarboniferous-Early Permian and Triassic) recognized alongthe northern margin of the NCC.

(2) The textures, mineral assemblages and whole-rock chemicaldata suggest that the Longwangmiao intrusion formedthrough fractional crystallization and crystal accumulationfrom an anhydrous, island-arc picritic ankaramite magma,which was generated by low degree partial melting ofgarnet-peridotite facies at the boundary of slightly enrichedsub-continental lithospheric mantle and crust. The magmaevolved into basaltic in composition through incorporationof silica-rich crustal materials in subduction setting andbecame hydrated through the release of fluids from thedown going oceanic slab.

(3) The scarcity of orthopyroxene and plagioclase and accumula-tion of pyroxene and hornblende in the Longwangmiao intru-sion are consistent with the features of Alaskan-typeultramafic–mafic intrusions, which are consider as arc mag-matic rocks in active convergent margin. The arc signature ofLongwangmiao rocks is further supported by their geochemi-cal features suggesting their formation in a convergent marginwhere the Mongolian oceanic slab subducted beneath the NCC.The final emplacement of the arc Longwangmiao intrusion waslinked to a geodynamic setting that switched from arc-relatedcompression to back-arc extension as evidenced by their dualIAB and CRB signature. The post-collisional extensional settingowe to the arc-continental collision between the Bainaimiaoarc and the northern NCC during the Late Silurian.

Acknowledgements

We thank Guest Editor Prof. Toshiaki Tsunogae and two anony-mous referees for helpful and constructive comments. This studyforms part of the doctoral research of X.M. Teng at the ChinaUniversity of Geosciences Beijing. Funding for this study was pro-vided through the Talent Award project to M. Santosh throughthe 1000 Talents Plan of the Chinese Government and the Projectto M. Santosh from Open Fund of SKLCD of the NorthwestUniversity, China. We also thank Qiongyan Yang, Xiaofang He and

Li Tang for their kindly help in both field investigation and experi-mental work.

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.2015.04.032.

References

Agrawal, S., Guevara, M., Verma, S.P., 2008. Tectonic discrimination of basic andultrabasic volcanic rocks through log-transformed ratios of immobile traceelements. Int. Geol. Rev. 50, 1057–1079.

Amelin, Y., Lee, D.C., Halliday, A.N., 2000. Early-Middle Archaean crustal evolutiondeduced from Lu–Hf and U–Pb isotopic studies of single zircon grains. Geochim.et Cosmochim. Acta 64, 4205–4225.

Anderson, T., 2002. Correction of common Pb in U–Pb analyses that do not report204Pb. Chem. Geol. 192, 59–79.

Attoh, K., Evans, M.J., Bickford, M.E., 2006. Geochemistry of an ultramafic-rodingiterock association in the Paleoproterozoic Dixcove greenstone belt, southwesternGhana. J. Afr. Earth Sci. 45, 333–346.

Batanova, V.G., Pertsev, A.N., Kamenetsky, V.S., Ariskin, A.A., Mochalov, A.G.,Sobolev, A.V., 2005. Crustal evolution of island-arc ultramafic magma:galmoenanpyroxenite–dunite plutonic complex, Koryak highland (Far EastRussia). J. Petrol. 46, 1345–1366.

BlichertToft, J., Albarede, F., 1997. The Lu–Hf isotope geochemistry of chondritesand the evolution of the mantle–crust system. Earth Planet. Sci. Lett. 148, 243–258.

Bogaard, P.F.J., Wörner, G., 2003. Petrogenesis of basanitic to tholeiitic volcanicrocks from the Miocene Vogelsberg, Central Germany. J. Petrol. 44, 569–602.

Chardon, D., 2003. Strain partitioning and batholith emplacement at the root of atranspressive magmatic arc. J. Struct. Geol. 25, 91–107.

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., Tian, W., Jahn, B.M., Chen, Z.C., 2008. Zircon SHRIMP U–Pb ages and in-situHf isotopic analysis for the Mesozoic intrusions in South Taihang, North Chinacraton: evidence for hybridization between mantle-derived magmas andcrustal components. Lithos 102, 118–137.

Chen, B., Jahn, B.M., Tian, W., 2009a. 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. J. Asian Earth Sci. 34, 245–257.

Chen, B., Suzuki, K., Tian, W., Jahn, B.M., Ireland, T., 2009b. Geochemistry and Os–Nd–Sr isotopes of the Gaositai Alaskan-type ultramafic complex from thenorthern North China craton: implications for mantle–crust interaction.Contrib. Miner. Petrol. 158, 683–702.

Chu, N.C., Taylor, R.N., Chavagnac, V., Nesbitt, R.W., Boela, R.M., Milton, J.A.,Germain, C.R., Bayon, G., Burton, K., 2002. Hf isotope ratio an analysis usingmulti-collector inductively coupled plasma mass spectrometry: an evaluationof isobaric interference corrections. J. Anal. At. Spectrom. 17, 1567–1574.

Corfu, F., Hanchar, J.M., Hoskin, P.W., Kinny, P., 2003. Atlas of zircon textures. Rev.Mineral. Geochem. 53, 469–500.

Davies, J.F., Grant, R.W.E., Whitehead, R.E.S., 1979. Immobile trace elements andArchean volcanic stratigraphy in the Timmins mining area, Ontario. Can. J. EarthSci. 16, 305–311.

Davis, G.A., Zheng, Y.D., Wang, C., Darby, B.J., Zhang, C.H., Gehrels, G.E., 2001.Mesozoictectonic evolution of the Yanshan fold and thrust belt, with emphasison Hebeiand Liaoning Provinces, Northern China. In: Hendrix, M.S., Davis, G.A.(Eds.), Paleozoic and Mesozoic Tectonic Evolution of Central Asia: FromContinental Assembly to Intracontinental Deformation, vol. 194. GeologicalSociety of America Memoir, pp. 171–197.

DeBievre, P., Taylor, P.D.P., 1993. Table of the isotopic composition of the elements.Int. J. Mass Spect. Ion Process 123, 149–166.

Deng, Y., Yuan, F., Zhou, T., Xu, C., Zhang, D., Guo, X., 2013. characteristics andtectonic setting of the Tuerkubantao mafic-ultramafic intrusion in WestJunggar, Xinjiang, China. Geosci. Front. http://dx.doi.org/10.1016/j.gsf.2013.10.003.

Eyuboglu, Y., Dilek, Y., Bozkurt, E., Bektas, O., Rojay, B., Sen, C., 2010. Structure andgeochemistry of an Alaskan-type ultramafic–mafic complex in the EasternPontides, NE Turkey. Gondwana Res. 18, 230–252.

Frey, F.A., Prinz, M., 1978. Ultramafic inclusions from San Carlos, Arizona: petrologicand geochemical data bearing on their petrogenesis. Earth Planet. Sci. Lett. 38,129–176.

Furman, T., 1995. Melting of metasomatized subcontinental lithosphereundersaturated mafic lavas from Rungwe, Tanzania. Contrib. Miner. Petrol.122, 97–115.

Gao, S., Rudnick, R.L., Xu, W.L., Yuan, H.L., Liu, Y.S., Walker, R.J., Puchtel, I.S., Liu, X.,Huang, H., Wang, X.R., Yang, J., 2008. Recycling deep cratonic lithosphere andgeneration of intraplate magmatism in the North China Craton. Earth Planet.Sci. Lett. 270, 41–53.



http://refhub.elsevier.com/S1367-9120(15)00241-2/h0005























































http://dx.doi.org/10.1016/j.gsf.2013.10.003

http://dx.doi.org/10.1016/j.gsf.2013.10.003















Green, D.H., Edgar, A.D., Beasley, P., Kiss, E., Ware, N.G., 1974. Upper mantle sourcefor some hawaiites, mugearites and benmoreites. Contrib. Miner. Petrol. 48, 33–43.

Green, D.H., Schmidt, M.W., Hibberson, W.O., 2004. Island-arc ankaramites:primitive melts from fluxed refractory lherzolitic mantle. J. Petrol. 45, 391–403.

Griffin, W.L., Pearson, N.J., Belousova, E., Jackson, S.E., van Achterbergh, E., O’Reilly,S.Y., Shee, S.R., 2000. The Hf isotope composition of cratonic mantle: LA-MC-ICPMS analysis of zircon megacrysts in kimberlites. Geochim. et Cosmochim.Acta 64, 133–147.

Griffin, W.L., Wang, X., Jackson, S.E., Pearson, N.J., O’Reilly, S.Y., Xu, X., Zhou, X., 2002.Zircon chemistry and magma mixing, SE China: in-situ analysis of Hf isotopes,Tonglu and Pingtan igneous complexes. Lithos 61, 237–269.

Hawkesworth, C., Ellam, R., 1989. Chemical fluxes and wedge replenishment ratesalong recent destructive plate margins. Geology 17, 46–49.

HBGMR (Hebei Bureau of Geology and Mineral Resources), 1989. Regional geologyof Hebei Province, Beijing Municipality and Tianjin Municipality: Beijing,Geological Publishing House, 741 p. (in Chinese with English abstract).

Helmy, H.M., El Mahallawi, M.M., 2003. Gabbro Akarem mafic-ultramafic complex,Eastern Desert, Egypt: a Late Precambrian analogue of Alaskan-type complexes.Mineral. Petrol. 77, 85–108.

Himmelberg, G.R., Loney, R.A., 1995. Characteristics and Petrogenesis of Alaskan-type Ultramafic-Mafic Intrusions, Southeastern Alaska. US Government PrintingOffice, p. 47.

Hofmann, A.W., 1988. Chemical differentiation of the earth: the relationshipbetween mantle, continental crust and oceanic crust. Earth Planet. Sci. Lett. 90,297–314.

Hsu, K.J., Wang, Q., Li, J., Hao, J., 1991. Geologic evolution of the Neimonides: aworking hypothesis. Eclogae Geol. Helv. 84, 1–31.

Hu, X., Xu, C., Niu, S., 1990. Evolution of the Early Paleozoic Continental MargininNorthern Margin of the North China Platform. Peking University Publish House,Beijing, p. 216 (in Chinese with English abstract).

Huang, T.K., 1945. On major tectonic forms of China: National Geological Survey ofChina Geological Memoir (Ser. A), vol. 20, 165 p.

Irvine, T.N., Baragar, W.R.A., 1971. A guide to the chemical classification of thecommon volcanic rocks. Can. J. Earth Sci. 8, 523–548.

Irvine, T.N., 1974. Petrology of the Duke Island ultramafic complex southeasternAlaska. Geol. Soc. Am. Mem. 138, 1–244.

Irving, A.J., 1980. Petrology and geochemistry of composite ultramafic xenoliths inalkali basalts and implications for magmatic processes within the mantle. Am. J.Sci. 280, 389–426.

Irving, A.J., Frey, F.A., 1984. Trace element abundances in megacrysts and their hostbasalts: constraints on partition coefficients and megacryst genesis. Geochim.et Cosmochim. Acta 48, 1201–1221.

Ishiwatari, A., Ichiyama, Y., 2004. Alaskan-type plutons and ultramafic lavas in FarEast Russia, Northeast China, and Japan. Int. Geol. Rev. 46, 316–331.

Jahn, B.M., Wu, F.Y., Chen, B., 2000. Granitoids of the Central Asian Orogenic Belt andcontinental growth in the Phanerozoic. Geol. Soc. Am. Special Papers 350, 181–193.

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.

Jiang, N., 2005. Petrology and geochemistry of the Shuiquangou syenitic complex,northern margin of the North China Craton. J. Geol. Soc., Lond. 162, 203–215.

Johan, Z., 2006. Platinum-group minerals from placers related to the NizhniTagil(Middle Urals, Russia) Uralian–Alaskan-typeultramafic complex: ore-mineralogy and study of silicate inclusionsin (Pt, Fe) alloys. Mineral. Petrol.87, 1–30.

Jourdan, F., Bertrand, H., Schärer, U., BlichertToft, J., Fëraud, G., Kampunzu, A.B.,2007. Major and trace elements and Sr, Nd, Hf, and Pb isotope compositions ofthe Karoo Large Igneous Province, Botswana-Zimbabwe: lithosphere vs. mantleplume contribution. J. Petrol. 48, 1043–1077.

Jung, C., Jung, S., Hoffer, E., Berndt, J., 2006. Petrogenesis of Tertiary mafic alkalinemagmas in the Hocheifel, Germany. J. Petrol. 47, 1637–1671.

Kelemen, P.B., 1995. Genesis of high Mg# andesites and the continental crust.Contrib. Miner. Petrol. 120, 1–19.

Kelemen, P.B., Hart, S.R., Bernstein, S., 1998. Silica enrichment in the continentalupper mantle via melt/rock reaction. Earth Planet. Sci. Lett. 164, 387–406.

Kinzler, R.J., 1997. Melting of mantle peridotite at pressures approaching the spinelto garnet transition: application to mid-ocean ridge basalt petrogenesis. J.Geophys. Res. 102, 853–874.

Kuno, H., 1968. Origin of andesite and its bearing on the island arc structure. Bull.Volcanol. 32, 141–176.

Langmuir, C.H., Klein, E.M., Plank, T., 1992. Petrological systematics of mid-oceanridge basalts: constraints on melt generation beneath ocean ridges. In: Morgan,J.P., Blackman, D.K., Sinton, J.M. (Eds.), Mantle Flow and Melt Generation at Mid-ocean Ridges. Geophysical Monograph, American Geophysical Union, vol. 71,pp. 183–280.

LBGMR (Liaoning Bureau of Geology and Mineral Resources), 1989. Regionalgeology of Liaoning Province. Geological Publishing House, Beijing (in Chinesewith English abstract)

Leake, B.E., Woolley, A.R., Arps, C.E.S., Birch, W.D., Gilbert, M.C., Grice, J.D.,Hawthorne, F.C., Kato, A., Kisch, H.J., Krivovichev, V.G., Linthout, K., Laird, J.,Mandarino, J.A., Maresch, W.V., Nickel, E.H., Rock, N.M.S., Schumacher, J.C.,Smith, D.C., Stephenson, N.C.N., Ungaretti, L., Whittaker, E.J.W., Guo, Y., 1997.Nomenclature of amphiboles: report of the subcommittee on amphiboles of the

international mineralogical association, commission on new minerals andmineral names. Am. Mineral. 82, 1019–1037.

Li, J.Y., Zhang, J., Yang, T.N., et al., 2009. Crustal tectonic division and evolution of thesouthern part of the North Asian Orogenic Regionandits adjacent areas. J. JilinUniv. (Earth Science ed.) 39, 584–605 (in Chinese with English abstract).

Lindsley, D.H., 1983. Pyroxene thermometry. Am. Mineral. 68, 477–493.Liu, D.Y., Nutman, A.P., Compston, W., Wu, J.S., Shen, Q.H., 1992. Remnants of

3800 Ma crust in the Chinese part of the Sino-Korean Craton. Geology 20, 339–342.

Liu, D.Y., Jian, P., Zhang, Q., Zhang, F.Q., Shi, Y.R., Shi, G.H., Zhang, L.Q., Tao, H., 2003.SHRIMP dating of adakites in the Tulingkaiophiolite, Inner Mongolia: Evidencefor the Early Paleomic subduction. Acta Geol. Sinica 77, 317–327 (in Chinesewith English abstract).

Liu, J.M., Zhao, Y., Liu, X.M., Liu, X.W., 2007. Sedimentation feature and its tectonicsignificances of Xingshikou formation in Xiabancheng Basin, Yanshan fold-andthrustbelt. Acta Petrol. Sinica 23, 639–654 (in Chinese with English abstract).

Liu, J.M., Zhao, Y., Sun, Y.L., Li, D.P., Liu, J., Chen, B.L., Zhang, S.H., Sun, W.D., 2010.Recognition of the latest Permian to Early Triassic Cu–Mo mineralization on thenorthern margin of the North China block and its geological significance.Gondwana Res. 17, 125–134.

Liu, S.W., Lü, Y.J., Wang, W., Yang, P.T., Bai, X., Feng, Y.G., 2011. Petrogenesis of theNeoarchean granitoid gneisses in northern Hebei Province. Acta Petrol. Sinica27, 909–921 (in Chinese with English abstract).

Luo, Z.K., Miao, L.C., Guan, K., Qiu, Y.S., Qiu, M.Y., McNaughton, N.J., Groves, D.I.,2001. SHRIMP chronological study of the Shuiquangou intrusive body inZhangjiakou area, Hebei Province and geochemical significance. Geochimica 30,116–122 (in Chinese with English abstract).

McCulloch, M.T., Gamble, A.J., 1991. Geochemical and geodynamical constraints onsubduction zone magmatism. Earth Planet. Sci. Lett. 102, 358–374.

Miller, R.B., Paterson, S.R., Matzel, J.P., 2009. Plutonism at different crustal levels:insights from the 5–40 km (paleo depth) North Cascades crustal section,Washington. In: Miller, R.B., Snoke, A.W. (Eds.), Crustal Cross Sections from theWestern North American Cordillera and Elsewhere: Implications for Tectonicand Petrologic Processes. Geological Society of America Special Paper, 456, pp.125–149.

Needy, S.K., Anderson, J.L., Wooden, J.L., Barth, A.P., Paterson, S.R., Memeti, V.,Pignotta, G.S., 2009. Mesozoic magmatism in an upper- to middle-crustalsection through the Cordilleran continental margin arc, eastern TransverseRanges, California. In: Miller, R.B., Snoke, A.W. (Eds.), Crustal Cross Sectionsfrom the Western North American Cordillera and Elsewhere: Implications forTectonic and Petrologic Processes. Geological Society of America Special Paper,456, pp. 187–218.

Ni, Z.Y., 2002. Retrograded eclogites, rodingites and metamorphic periodtites andtheir geotectonic significance m the northern margin ofthe North China craton,Hebei Province, China[D]. Postdoct oral research report of the Institute ofGeology and Geophysics, Chinese Academy of Sciences, pp. 1–83 (in Chinesewith English abstract).

Pan, Y., 1996. Early Permian Bajiazi ultra-unit intrusive rock and its emplacementmechanism, Jianping area. Liaoning Geol. 14, 284–292 (in Chinese with Englishabstract).

Peate, D.W., 1997. The Paraná-Etendeka Province. In: Mahoney, J.J., Coffin, M.F.(Eds.), Large Igneous Provinces, Geophysical Monograph 100. AmericanGeophysical Union, Washington, DC, pp. 217–245.

Robinson, P.T., Zhou, M.F., Hu, X.F., Reynolds, P., Bai, W., Yang, J., 1999. Geochemicalconstraints on the origin of the Hegenshan Ophiolite, Inner Mongolia, China. J.Asian Earth Sci. 17, 423–442.

Roeder, P.L., Emslie, R., 1970. Olivine-liquid equilibrium. Contrib. Miner. Petrol. 29,275–289.

Safonova, I.Yu., Santosh, M., 2014. Accretionary complexes in the Asia-Pacificregion: tracing archives of ocean plate stratigraphy and tracking mantleplumes. Gondwana Res. 25, 126–158.

Santosh, M., 2010. Assembling North China Craton within the Columbiasupercontinent: the role of double-sided subduction. Precambr. Res. 178,149–167.

Santosh, M., Yang, Q.Y., Teng, X.M., Tang, L., 2015. Paleoproterozoic crustal growthin the North China Craton: evidence from the Lüliang Complex. Precambr. Res.http://dx.doi.org/10.1016/j.precamres.2015.03.015.

Saunders, A.D., Norry, M.J., Tarney, J., 1991. Fluid influence on the trace-elementcompositions of subduction zone magmas. Philosoph. Transact. Roy. Soc. Lond.Ser. A – Math. Phys. Eng. Sci. 335, 377–392.

Saunders, A.D., Storey, M., Kent, R.W., Norry, M.J., 1992. Consequences of plume–lithosphere interactions. In: Alabaster, T., Storey, B.C., Pankhurst, R.J. (Eds.),Magmatism and the Causes of Continental Break-up. Geological Society,London, Special Publications, vol. 68, pp. 41–60.

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

Schnetzler, C.C., Philpotts, J.A., 1970. Partition coefficients of rare-earth elementsbetween igneous matrix material and rock-forming mineral phenocrysts – II.Geochim. et Cosmochim. Acta 34, 331–340.

Shi, Y.R., Liu, D.Y., Miao, L.C., Zhang, F.Q., Jian, P., Zhang, W., Hou, K.J., Xu, J.Y., 2010.Devonian A-type granitic magmatism on the northern margin of the NorthChina Craton: SHRIMP U–Pb zircon dating and Hf-isotopes of the Hongshangranite at Chifeng, Inner Mongolia, China. Gondwana Res. 17, 632–641.

Sisson, T.W., Grove, T.L., 1993. Experimental investigations of the role of H2O incalcalkaline differentiation and subduction zone magmatism. Contribut.Mineral. Petrol. 113, 143–166.


























































































































http://dx.doi.org/10.1016/j.precamres.2015.03.015


















Snoke, A.W., Quick, J.E., Bowman, H.R., 1981. Bear Mountain igneous complex,Klamath Mountains, California: an ultrabasic to silicic calkalkaline suite. J.Petrol. 22, 501–552.

Söderlund, U., Patchett, P.J., Vervoort, J.D., Isachsen, C.E., 2004. The 176Lu decayconstant determined by Lu–Hf and U–Pb isotope systematics of Precambrianmafic intrusions. Earth Planet. Sci. Lett. 219, 311–324.

Song, B., Allen, P.N., Liu, D.Y., Wu, J.S., 1996. 3800 to 2500 Ma crustal evolution inthe Anshan area of Liaoning Province, northeastern China. Precambr. Res. 78,79–94.

Suen, C.J., Frey, F.A., 1987. Origins of the mafic and ultramafic rocks in the Rondaperidotite. Earth Planet. Sci. Lett. 85, 183–202.

Sun, S.S., McDonough, W.F., 1989. Chemical and isotopic systematics of oceanicbasalts: implications for mantle composition and process. In: Saunders, A.D.,Nony, M.J. (Eds.), Magmatism in the Ocean Basin: Geological Society LondonSpecial Publication, vol. 42, pp. 313–354.

Tang, K., Yan, Z., 1993. Regional metamorphism and tectonic evolution of the InnerMongolia suture zone. J. Metamorph. Geol. 11, 511–522.

Tang, Y.J., Zhang, H.F., Santosh, M., Ying, J.F., 2013. Differential destruction of theNorth China Craton: a tectonic perspective. J. Asian Earth Sci. 78, 71–82.

Taylor, H.P., 1967. The zoned ultramafic complexes of southeastern Alaska. In:Wyllie, P.J. (Ed.), Ultramafic and Related Rocks. Wiley, New York, pp. 97–121.

Teng, X.M., Santosh, M., 2015. A long-lived magma chamber in the PaleoproterozoicNorth China Craton: evidence from the Damiao gabbro-anorthosite suite.Precambr. Res. 256, 79–101.

Thieblemont, D., Tegyey, M., 1994. Geochemical discrimination of differentiatedmagmatic rocks attesting for the variable origin and tectonic setting of calc-alkaline magmas. Comptes Rendus De L Academie Des Sciences Serie II 319, 87–94.

Thirlwall, M.F., Upton, B.G.J., Jenkins, C., 1994. Interaction between continentallithosphere and the Iceland plume: Sr–Nd–Pb isotope chemistry of Tertiarybasalts, NE Greenland. J. Petrol. 35, 839–897.

Tian, W., Chen, B., Liu, C.Q., Zhang, H.F., 2007. Zircon U–Pb age and Hf isotopiccomposition of the Xiaozhangjiakou ultramafic pluton in northern Hebei. ActaPetrol. Sinica 23, 583–590 (in Chinese with English abstract).

Tistl, M., Burgath, K.P., Höhndorf, A., Kreuzer, H., Munoz, R., Salinas, R., 1994. Originand emplacement of Tertiary ultramafic complexes in northwest Colombia:Evidence from geochemistry and K Ar, Sm Nd and Rb�Sr isotopes. Earth Planet.Sci. Lett. 126, 41–59.

Van Westrenen, W., Blundy, J.D., Wood, B.J., 2001. High field strength element/rareearth element fractionation during partial melting in the presence of garnet:implications for identification of mantle heterogeneities. Geochem. Geophys.Geosyst. 2, 200GC000133.

Vervoort, J.D., Patchett, P.J., 1996. Behavior of hafnium and neodymium isotopes inthe crust: Constraints from Precambrian crustally derived granites. Geochim. etCosmochim. Acta 60, 3717–3733.

Wan, B., Hegner, E., Zhang, L.C., Rocholl, A., Chen, Z.G., Wu, H.Y., Chen, F.K., 2009.Rb–Sr geochronology of chalcopyrite from the Chehugou porphyry Mo–Cudeposit (Northeast China) and geochemical constraints on the origin of hostinggranites. Econ. Geol. 104, 351–363.

Wilson, B.M., 1989. Igneous Petrogenesis a Global Tectonic Approach. Chapman &Hall, London, p. 466.

Winchester, J.A., Floyd, P.A., 1976. Geochemical magma type discrimination:application to altered and metamorphosed basic igneous rocks. Earth Planet.Sci. Lett. 28, 459–469.

Windley, B.F., Alexeiev, D., Xiao, W., Kröner, A., Badarch, G., 2007. Tectonic modelsfor accretion of the Central Asian Orogenic Belt. J. Geol. Soc., Lond. 164, 31–47.

Woodhead, J., Hergt, J., Shelley, M., Eggins, S., Kemp, R., 2004. Zircon Hf-isotopeanalysis with an excimer laser, depth profiling, ablation of complex geometries,and concomitant age estimation. Chem. Geol. 209, 121–135.

Wu, F.Y., Li, X.H., Zheng, Y.F., Gao, S., 2007. Lu–Hf isotopic systematics and theirapplications in petrology. Acta Petrol. Sinica 23, 185–220 (in Chinese withEnglish abstract).

Xiao, W., Windley, B.F., Hao, J., Zhai, M.G., 2003. Accretion leading to collision andthe Permian Solonker suture, Inner Mongolia, China: termination of the centralAsianorogenic belt. Tectonics 22, 1069.

Xiao, W., Han, C., Liu, W., Wan, B., Zhang, J., Ao, S., Zhang, Z., Song, D., Tian, Z., Luo, J.,2014. How many sutures in the southern Central Asian Orogenic Belt: Insightsfrom East Xinjiang-West Gansu (NW China)? Geosci. Front. 5, 525–536.

Xiao, W.J., Santosh, M., 2014. The western Central Asian Orogenic Belt: a window toaccretionary orogenesis and continental growth. Gondwana Res. 25, 1429–1444.

Xu, B., Chen, B., 1997. Framework and evolution of the middle Paleozoicorogenicbelt between Siberian and north China plates in northern InnerMongolia. Sci.China (Ser. D) 40, 463–479.

Yang, J.H., Wu, F.Y., Chung, S.L., Wilde, S.A., Chu, M.F., 2006a. A hybrid origin for theQianshan A-type granite, northeast China: geochemical and Sr–Nd–Hf isotopicevidence. Lithos 89, 89–106.

Yang, J.H., Wu, F.Y., Shao, J.A., Xie, L.W., Liu, X.M., 2006b. In-situ U–Pb dating and Hfisotopic analyses of zircons from volcanic rocks of the Houcheng andZhangjiakou Formations in the Zhuang-Xuan area, northeast China. Earth Sci.-J. China Univ. Geosci. 31, 71–80 (in Chinese with English abstract).

Yang, Q.Y., Santosh, M., 2014. Paleoproterozoic arc magmatism in the North ChinaCraton: No Siderian global plate tectonic shutdown. Gondwana Res. http://dx.doi.org/10.1016/j.gr.2014.08.005.

Yang, Q.Y., Santosh, M., 2015. Charnockite magmatism during a transitional phase:Implications for Late Paleoproterozoic ridge subduction in the North ChinaCraton. Precambr. Res. http://dx.doi.org/10.1016/j.precamres.2015.01.014.

Ye, H., Zhang, S.H., Zhao, Y., Liu, J.M., He, Z.F., 2014. Recognition of the latestDevonian volcanic rocks in Chifeng area, northern North China block, and itsgeological implications. Geol. Bull. China 33, 1274–1283 (in Chinese withEnglish abstract).

Yuan, H.L., Gao, S., Liu, X.M., Li, H.M., Gunther, D., Wu, F.Y., 2004. Accurate U–Pb ageand trace element determination of zircon by laser ablation-inductivelycoupled plasma-mass spectrometry. Geostand. Geoanal. Res. 28, 353–370.

Yuan, H.L., Gao, S., Dai, M.N., Zong, C.L., Günther, D., Fontaine, G.H., Liu, X.M., Diwu,C.R., 2008. Simultaneous determinations of U–Pb age, Hf isotopes and traceelement compositions of zircon by excimer laser-ablation quadrupole andmultiple-collector ICP-MS. Chem. Geol. 247, 100–118.

Zák, J., Verner, K., Johnson, K., Schwartz, J.J., 2012. Magnetic fabric of Late Jurassicarc plutons and kinematics of terrane accretion in the Blue Mountains,northeastern Oregon. Gondwana Res. 22, 341–352.

Zhai, M.G., 2014. Multi-stage crustal growth and cratonization of the North ChinaCraton. Geosci. Front. 5, 457–459.

Zhai, M.G., Santosh, M., 2011. The early Precambrian odyssey of the North ChinaCraton: a synoptic overview. Gondwana Res. 20, 6–25.

Zhai, M.G., Santosh, M., 2013. Metallogeny of the North China Craton: link withsecular changes in the evolving Earth. Gondwana Res. 24, 275–297.

Zhang, C., (Master of Science Thesis) 2013. Rock association, zircon U–Pbgeochronology of Bainaimiao Group in SonidYouqi, Inner Mongolia and itsgeological significance. Jilin University, Changchun (in Chinese).

Zhang, H.F., Yang, Y.H., 2007. Emplacement age and Sr–Nd–Hf isotopiccharacteristics of the diamondiferous kimberlites from the eastern NorthChina Craton. Acta Petrol. Sinica 23, 285–294 (in Chinese with English abstract).

Zhang, S.H., Zhao, Y., Song, B., 2006. Hornblende thermobarometry of theCarboniferous granitoids from the Inner Mongolia paleo-uplift: implicationsfor the geotectonic evolution of the northern margin of North China block.Mineral. Petrol. 87, 123–141.

Zhang, S.H., Zhao, Y., Song, B., Liu, D.Y., 2007a. Petrogenesis of the Middle DevonianGushan diorite pluton on the northern margin of the North China block and itstectonic implications. Geol. Mag. 144, 553–568.

Zhang, S.H., Zhao, Y., Song, B., Yang, Z.Y., Hu, J.M., Wu, H., 2007b. Carboniferousgranitic plutons from the northern margin of the North China block:implications for a late Paleozoic active continental margin. J. Geol. Soc. 164,451–463.

Zhang, S.H., Zhao, Y., Kröner, A., Liu, X.M., Xie, L.W., Chen, F.K., 2009a. Early Permianplutons from the northern North China Block: constraints on continental arcevolution and convergent margin magmatism related to the Central AsianOrogenic Belt. Int. J. Earth Sci. 98, 1441–1467.

Zhang, S.H., Zhao, Y., Liu, X.C., Liu, D.Y., Chen, F., Xie, L.W., Chen, H.H., 2009b. LatePaleozoic to Early Mesozoic mafic–ultramafic complexes from the northernNorth China Block: constraints on the composition and evolution of thelithospheric mantle. Lithos 110, 229–246.

Zhang, S.H., Zhao, Y., Song, B., Hu, J.M., Liu, S.W., Yang, Y.H., Liu, J., 2009c.Contrasting Late Carboniferous and Late Permian-Middle Triassic intrusivesuites from the northern margin of the North China craton: geochronology,petrogenesis, and tectonic implications. Geol. Soc. Am. Bull. 121, 181–200.

Zhang, S.H., Zhao, Y., 2013. Mid-crustal emplacement and deformation of plutons inan Andean-style continental arc along the northern margin of the North ChinaBlock and tectonic implications. Tectonophysics 608, 176–195.

Zhang, W., Jian, P., 2008. SHRIMP dating of Early Paleozoic granites from NorthDamaoqi, Inner Mongolia. Acta Geol. Sinica 82, 778–787 (in Chinese withEnglish abstract).

Zhao, G.C., Cawood, P.A., 2012. Precambrian geology of China. Precambr. Res. 222,13–54.

Zhao, G.C., Wilde, S.A., Li, S.Z., Sun, M., Grant, M.L., Li, X.P., 2007. U–Pb zircon ageconstraints on the Dongwanzi ultramafic–mafic body, North China, confirm it isnot an Archean ophiolite. Earth Planet. Sci. Lett. 255, 85–93.

Zhao, G.C., Zhai, M.G., 2013. Lithotectonic elements of Precambrian basement in theNorth China Craton: review and tectonic implications. Gondwana Res. 23,1207–1240.

Zhao, T.P., Chen, W., Zhou, M.F., 2009. Geochemical and Nd–Hf isotopic constraintson the origin of the �1.74-Ga Damiaoanorthosite complex. North China Craton.Lithos 113, 673–690.

















































































http://dx.doi.org/10.1016/j.gr.2014.08.005

http://dx.doi.org/10.1016/j.gr.2014.08.005

http://dx.doi.org/10.1016/j.precamres.2015.01.014

































































journal of asian earth sciences€¦ · bdepartment of earth sciences, university of adelaide, sa...

Documents