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Solid Earth Sciences 4 (2019) 150e158

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Mantle xenoliths and host basalts record the Paleo-Asian oceanic materialsin the mantle wedge beneath northwest North China Craton

Hong-Kun Dai a,b, Jian-Ping Zheng a,*

a State Key Laboratory of Geological Processes and Mineral Resources, School of Earth Sciences, China University of Geosciences, Wuhan, 430074, Chinab Australian Research Council Centre of Excellence for Core to Crust Fluid Systems/GEMOC, Department of Earth and Planetary Sciences, Macquarie University,

Sydney, NSW 2109, Australia

Received 19 August 2019; revised 19 September 2019; accepted 20 September 2019

Available online 7 December 2019

Abstract

Oceanic subduction is an important trigger for mantle heterogeneity, which further increases melt production and controls the compositionsof intraplate basalts. Such a role played by the (Paleo-) Pacific subduction have been extensively studied and well constrained based on thewidespread mantle xenoliths and intraplate magmatism in the eastern North China Craton. By contrast, the recycled materials from otherPhanerozoic subducted slabs beneath the craton are relatively poorly recognized. Here, a reappraisal is made to the recently reported peridotitexenoliths and ~89 Ma host basalts from the Langshan area in the northwest North China Craton and regional data on xenoliths and basalts, withthe emphasis on the mass transfer in the mantle wedge from the subducted Paleo-Asian oceanic slab. The Langshan peridotites are fertile incomposition and record complex melt extraction and metasomatism. One episode of metasomatism is likely induced by silicate melts withconcomitant enrichments in large ion lithophile elements and high field strength elements and positive Eu anomaly, suggestive of the contri-bution from recycled materials. This metasomatism should take place in Paleozoic according to the diffusion modelling. The host basalts arecomparable with partial melts of pyroxenite under 2e3 GPa and have oceanic island basalts-like trace-element compositions. Positive Sr and Euanomalies, low Rb/Sr and high Ba/Rb ratios, and the moderated depleted but slightly decoupled SreNd isotopes suggest the involvement ofsubducted oceanic crustal materials in the mantle source. The Pb isotopic compositions are best modeled by the mixing between depletedmantle, altered oceanic crust with minor young (<500 Ma) sediments. These basalts are interpreted to be partial melts of pyroxenite-bearingasthenosphere containing slab-derived materials. Collectively, the mantle wedge beneath the northwest part of the craton is pervasivelymodified by slab-derived melts. The infiltrating melts were gradually consumed by interaction with country peridotites of the melt conduit duringthe migration from the slab-asthenosphere contact. This mass transfer process triggered the formation of pyroxenite in the asthenosphere at highmelt/rock ratio and metasomatism in the lithospheric mantle at low melt-rock ratio. Considering this Paleozoic melt infiltration, the regionalgeological records and the tectonic locality, the recycled materials in the mantle wedge beneath northwest part of the craton are likely derivedfrom the subducted Paleo-Asian oceanic slab.Copyright © 2019, Guangzhou Institute of Geochemistry. Production and hosting by Elsevier B.V. This is an open access article under the CCBY-NC-ND license (http://creativecommons.org/licenses/by-nc-nd/4.0/).

Keywords: Mantle heterogeneity; Recycled materials; Northwest North China Craton; Paleo-asian oceanic slab

* Corresponding author. School of Earth Sciences, China University of

Geosciences, Wuhan, 430074, China. Fax: þ86 27 67883002.

E-mail address: jpzheng@cug.edu.cn (J.-P. Zheng).

Peer review under responsibility of Guangzhou Institute of Geochemistry.

https://doi.org/10.1016/j.sesci.2019.09.001

2451-912X/Copyright © 2019, Guangzhou Institute of Geochemistry. Production an

ND license (http://creativecommons.org/licenses/by-nc-nd/4.0/).

1. Introduction

Oceanic subduction is one of the most important mecha-nisms to introduce mantle heterogeneity (Hofmann, 1997;Herzberg, 2011). On the one hand, the melts/fluids releasedfrom the subducted slab could trigger various types of mantlemetasomatism (O’Reilly and Griffin, 2013) and introducemantle metasomatites (e.g., pyroxenite and hornblendite,

d hosting by Elsevier B.V. This is an open access article under the CC BY-NC-

151H.-K. Dai, J.-P. Zheng / Solid Earth Sciences 4 (2019) 150e158

Bodinier et al., 2008; Bali et al., 2018) in the mantle wedgebeyond the subducted slab. On the other hand, residual maficcrust could be presented as pyroxenites and/or eclogitescompositionally distinct from ambient mantle (Herzberg,2011). These heterogeneous portions could be preferentiallymelted and exert significant control on the composition ofintraplate basalts (Pilot et al., 2008; Rooney et al., 2017).

Mantle heterogeneity caused by recycled materials hasbeen recorded by widespread basalt-borne mantle xenoliths(Zheng et al., 2007; Zhang et al., 2008; Zheng, 2009; Wu etal., 2019) and intraplate basalts of the Late Mesozoic toCenozoic ages (Li et al., 2017; Xu et al., 2018) in the easternNorth China Craton (NCC, Fig. 1A). Together with the stag-nant Pacific slab beneath the eastern part of the craton (Huangand Zhao, 2006) that were assumed to present since the LateCretaceous (Liu et al., 2017), the recycled materials wereinferred to be derived from the subducted (Paleo-) Pacific slab(Liu et al., 2019). However, the eastern NCC is located in theoverlapping area affected by the Phanerozoic subductionsfrom three directions, including the subduction of the Paleo-Asian ocean from the north in the Paleozoic (Xiao et al.,2015), the subduction of the Paleo-Tethyan ocean and

Fig. 1. A) Tectonic sketch map of the North China Craton with localities of mantl

from Dai et al. (2019). B) Simplified tectonic map of the NCC and surrounding te

subsequent the Yangtze block from the south in the Paleozoicand Earth Mesozoic (Wu et al., 2009), and the subduction ofthe (Paleo-) Pacific from the east (Windley et al., 2010). Thismakes it difficult to evaluate the contributions of other sub-ducted slabs to the mantle modification and basalt genesis. Therecord about the influence of Paleo-Asian oceanic subductionon the deep lithosphere of the eastern NCC are the Xuhuaigarnet pyroxenite xenoliths that have Paleozoic zircon ages(~397 Ma, Liu et al., 2013) and extremely light Mg isotopes(Wang et al., 2016).

Recently, xenoliths-bearing alkali basalts of the LateCretaceous ages (~89 Ma) were reported in the Langshan area,the northwest NCC (Fig. 1A). This locality is far fromconvergent boundaries on the south and the east and thus ofgreat potential to record mantle heterogeneity triggered by thesubduction from the north. The xenoliths are fertile spinellherzolites with weak metasomatism (Dai et al., 2018) and thehost basalts are asthenosphere-derived partial melts underlyinga thin lithosphere, whose source contains significant compo-nents from subducted oceanic crust materials (Dai et al.,2019). In this contribution, a reappraisal is made to the peri-dotite xenoliths and host basalts, and regional data on mantle

e xenoliths and schematically spatial distribution of Cenozoic basalts adopted

ctonic units.

Fig. 2. REE patterns of type I (A) and type II (B) clinopyroxene in the

Langshan peridotites (Dai et al., 2019) normalized to C1 chondrite

(McDonough and Sun, 1995). The composition of residual clinopyroxene after

various degrees of batch melting are calculated according to the method

described by Johnson (1998) using the partition coefficients from Ionov et al.

(2002) and Sano and Kimura (2007).

152 H.-K. Dai, J.-P. Zheng / Solid Earth Sciences 4 (2019) 150e158

xenoliths and Cenozoic basalts, with emphasis on decodingthe melt infiltration processes from the subducted Paleo-Asianslab to the lithospheric mantle.

2. Geological setting

The NCC is one of the oldest cratons on Earth with con-tinental rocks older than 3.6 Ga (Liu et al., 1992; Zheng et al.,2004). It finalized cratonization by amalgamation of severalmicro blocks in the Late Archean (Zhai and Santosh, 2011) orby collision of the western and eastern Archean blocks alongthe Trans-North Orogenic Belt in the Paleoproterozoic(Fig. 1A, Zhao et al., 2001). Since then, this craton kepttectono-thermal quiescent manifested by thick and unde-formed strata until Late Mesozoic. The two Archean blockswitnessed distinct evolution since the Late Mesozoic. Theeastern block experienced vigorous magmatism (Zhang et al.,2014) and widespread deformation (Wang et al., 2011; Menget al., 2019) while the western one remained as a stablecraton with tectono-thermal events constrained to the margins(Zhang et al., 2009; Liu et al., 2018). In addition, mantle xe-noliths from the eastern block shows remarkable lithosphericthinning during the Mesozoic and replacement of old coldrefractory lithospheric mantle by young hot fertile one (Griffinet al., 1999; Zheng et al., 2007). The ancient craton mantlecould be partially preserved in the core of this craton (Zhenget al., 2001; Sun et al., 2012). By contrast, geophysical ob-servations suggest the preservation of thick and refractorymantle beneath the western part (Chen et al., 2014; He, 2015).Recently reported mantle xenoliths from the northwest marginof the craton indicated the presence of a thin and fertile lith-ospheric mantle, similar to the newly accreted one beneath theeastern NCC (Wu et al., 2017; Dai et al., 2018).

Surrounding the NCC are Phanerozoic collision/subductionzones (Fig. 1B). To the north is the Solonker suture zoneformed by the southward subduction of the Paleo-Asian oceanand subsequent collision between the Mongolia terrane andthe NCC at the end of Paleozoic (Xiao et al., 2015). To thesouth is the Qinling-Dabie-Sulu orogenic belt formed by thenorthward subduction of the Paleo-Tethys ocean and subse-quently Yangtze block (Li et al., 1993; Zheng et al., 2003).The subduction of (Paleo-) Pacific begun at ~ 170 Ma in theNortheast China (Xu et al., 2013) and then expanded to thewhole eastern China with anticlockwise rotation of the driftingdirection (Maruyama et al., 1997; Sun et al., 2007). Thesoutheastward retreating of the subduction zone and passivedrifting of the overriding plate since ~140 Ma formed the bigmantle wedge beneath the eastern NCC (Zheng and Dai,2018). The western leading edge of the stagnant (Paleo-) Pa-cific slab could be imaged in the mantle transition zonebeneath Trans-North Orogenic belt (Liu et al., 2017).

3. Mantle metasomatism with recycled oceanic crustmaterials

The Langshan peridotites are typical spinel lherzolites with~65 vol% olivine, ~20 vol% orthopyroxene, ~13 vol%

clinopyroxene and ~2 vol% spinel and show protogranular togranular mosaic texture. They are comparable to the residualperidotites in terms of phase modes and mineral compositions(Dai et al., 2018). For instance, the spinel tends to have lowCr# [Cr/(Cr þ Al), atomic ratio] and TiO2 contents, typical ofmelting residues. These could suggest that these peridotites arefree of metasomatism (Pearce et al., 2000; Ionov et al., 2002).According to the rare earth element (REE) patterns, the con-stituent clinopyroxene are divided into two types. The type Iclinopyroxene (major type) are usually characterized byincreasing depletion of incompatible elements (Fig. 2A) whilethe type II (minor type) show enrichments in incompatibleelements (Fig. 2B), including light REEs, large ion lithophileelements (LILEs) and high field strength elements (HFSEs)(Dai et al., 2018). Both types of clinopyroxene are indistin-guishable in major-element compositions and morphology andcould coexist in a single thin section.

The heavy REE contents of type I clinopyroxene areconsistent with the residue of 0e12% melt extraction whiletheir light REEs are generally enriched compared to the resi-dues at equal melting degrees (Fig. 2A and B). This suggeststhe presence of universal metasomatism in these peridotites,which preferentially rise up the concentrations of incompatibleelements (Verni�eres et al., 1997). In this regard, the left-

Fig. 3. A) Sr/Sr* (Sr/Sr* ¼ SrN/sqrt(PrN * NdN)) vs Eu/Eu* (Eu/Eu* ¼ EuN/

sqrt(SmN * GdN)), B) Rb/Sr vs Ba/Rb diagrams and C) SreNd compositions

of the Late Cretaceous to Cenozoic basalts from the northwest NCC adopted

from Dai et al. (2019). Also plotted are the mixing lines between the depleted

mantle (DM, Salters and Stracke, 2004), altered oceanic crust (AOC,

Rehkamper and Hofmann, 1997), average Ca-rich sediments (Plank and

Langmuir, 1998), and ancient sediments (~1.5 Ga, Rehkamper and

Hofmann, 1997) following Xu et al. (2017). The red line represents the

mixing between AOC and Ca-rich sediments and the pink line stands for the

mixing between AOC and ancient sediments. The green and blue lines denote

the mixing between the depleted mantle and AOC containing various

sediments.

153H.-K. Dai, J.-P. Zheng / Solid Earth Sciences 4 (2019) 150e158

leaning REE patterns of the type I clinopyroxene is likely theresult of later melt extraction because the light REEs usuallypreferentially enters into partial melts during mantle melting(Adam and Green, 2006). Given the coexistence of the twotypes of clinopyroxene (Dai et al., 2018), the enrichments ofincompatible elements in the type II clinopyroxene should betriggered by heterogeneously melt infiltration after thismelting event.

Both types of clinopyroxene have low La/Yb and compa-rable Ti/Eu ratios with low Ca/Al ratio (<5, Dai et al., 2018),consistent with metasomatism by silicate melts (Coltorti et al.,1999; Zong and Liu, 2018). For the type I clinopyroxene, thelow La/Yb and high Ti/Eu ratios are likely the artifact of thepost-metasomatism partial melting and thus could not be in-dicator of silicate metasomatism. Instead, the low Ca/Al ratioare robust diagnosis for silica metasomatism because partialmelting can slightly increase the Ca/Al ratio of residual cli-nopyroxene (Zong and Liu, 2018 and references therein). Inthis regard, the Ca/Al ratio of the type I clinopyroxene beforethe partial melting event should be very low, indicative of theinteraction with silicate melts. For the type II clinopyroxene,they usually show concomitant enrichments in LILEs andHFSEs with strongly fractionated REEs (Dai et al., 2018).These characteristics are reminiscent of a silicate metasomaticagent similar to Nb-rich basalts (Rolland et al., 2002; Wanget al., 2008), which is believed to contain materials fromsubducted slab (Hastie et al., 2011). In addition, positive Euanomaly in type II clinopyroxene is likely reminder ofplagioclase-rich precursor (Weill and Drake, 1973). Consid-ering the low pressure of plagioclase stability field (O’Neill,1981), the metasomatic agent with positive Eu anomaly islikely inherited from subducted oceanic lower crust (Jacobet al., 2003).

4. Recycled oceanic crust materials in the asthenosphere

Recycled oceanic crust materials are widely recognized inthe Langshan basalts (Dai et al., 2019) and regional Cenozoicbasalts (Guo et al., 2014, 2016; Xu et al., 2017; Pang et al.,2019), based on the oceanic island basalt-like trace-elementpatterns with apparent positive Sr and Eu anomalies (Fig. 3A)and high Ba/Rb ratio (Fig. 3B). In addition, the SreNd iso-topes show slightly decoupling by shifting from the mantlearray toward more radiogenic Sr isotopes than those of MORB(Fig. 3C). Given the low Rb/Sr ratios of these basalts, such adecoupling could be inherited from a mantle source containingaltered oceanic crust (Rehkamper and Hofmann, 1997).Similar decoupling was recognized in the regional pyroxenitexenoliths (Xu, 2002). Mixing modelling shows that the SreNdisotopes of the Mesozoic to Cenozoic alkali basalts from thenorthwest NCC could result from the mixing between depletedmantle and altered oceanic crust with ~6% sediments(Fig. 3C).

These basalts usually have low silica, high alkali contentsand are comparable to pyroxenite melts with a residual [Ol þCpx þ Gt] (Fig. 4A). Given that regional lithospheric mantleis overall fertile with depleted elements (Dai et al., 2018) and

isotopes (Choi et al., 2008) and contain enriched pyroxenites(Xu, 2002; Wei et al., 2018), both the lithospheric mantle andasthenosphere are possible candidates for the source of thesebasalts. Considering the lack of garnet peridotite xenoliths

Fig. 4. A) Projection of the primary melts of regional alkali basalts from or

towards Olivine into the plane CS-MS-A which is a larger portion of the

pyroxeneegarnet plane (thermal divide) and B) the melting conditions for

these basalts adopted from Dai et al. (2019). Also shown in B) are the tran-

sition line between the garnet to spinel facies peridotites (O’Neill, 1981) and

the melting contours of fertile peridotite (Katz et al., 2003). Fig. 5. A) Calculation of Th diffusion time in Langshan clinopyroxene with a

radius of 1000 mm. Given the Arrhenius parameters of Th diffusion in cli-

nopyroxene (Ea ¼ 356,000 J, log D0 ¼ �7.77, Van Orman et al., 1998), the Th

diffusion rate (D) can be calculated by D ¼ D0 exp(Ea/RT) (Cherniak and

Dimanov, 2010), where R is the molar gas constant (R ¼ 8.314 J/mol) and

T is temperature in Kelvin. For a given spherical crystal with radius a, the

minimum time scale necessary to affect the average composition of a crystal

can be calculated by tmin ¼ 0.001a2/D (s), and the maximum time scale

necessary to effectively homogenize the crystal can be calculated by

tmax ¼ 0.5a2/D (s) (Tomascak et al., 2016). The solid and dotted lines show the

correlation of the maximum and minimum time scale with temperature at

given mineral radius, respectively. The temperatures were calculated based on

FeeMg exchange between orthopyroxene and clinopyroxene (Brey and

K€ohler, 1990). B) Pb isotopic composition of the Langshan basalts. The

regional ophiolites of the Paleo-Asian ocean complied by Dai et al. (2019) are

also plotted for comparison (open circle). The Pb isotopes of present sub-

ducted sediments are calculated according to the two-stage evolution model

(Stacey and Kramers, 1975) with the first stage from 4.57 Ga to 3.7 Ga at

m ¼ 7.19 and the second stage from 3.7 Ga to present at m ¼ 9.9 (Kuritani

et al., 2011). The present Pb isotopes of ancient sediments are obtained by

radiogenic growth from their formation age to the present at m ¼ 2

(Rehkamper and Hofmann, 1997). The Pb content and isotopic composition of

depleted mantle, sediments and altered oceanic crust (AOC) are taken from

Rehkamper and Hofmann (1997), Kuritani et al. (2011) and Hauff et al.

(2003), respectively.

154 H.-K. Dai, J.-P. Zheng / Solid Earth Sciences 4 (2019) 150e158

(Dai et al., 2018) and the transition pressure of spinel to garnetfacies peridotite (O’Neill, 1981), the regional lithospheric baseshould have a pressure of ~ 2.2 GPa and a potential temper-ature of ~ 1350 �C (Fig. 4B), corresponding to a lithosphericthickness of 72 Km (Anderson, 1989). Estimated meltingpressures of these basalts (2e3 GPa) are consistent with thoseof the lithosphere base (Fig. 4B), in accordance with the lideffect that lithospheric thickness exert first-order control onthe compositions and melting pressure of intraplate basalts(Niu et al., 2011). In this regard, the high melting temperatures(Tp ¼ 1340e1450 �C) of these basalts could suggest anasthenosphere origin. Together the recognized recycledoceanic slab materials in these basalts, the inferred sourcepyroxenite (Fig. 4A) is likely generated by reaction of slab-derived melts and ambient peridotites.

5. Constraints on the time of melt infiltration in themantle wedge

Given that the mineral major elements of the Langshanperidotites are controlled by partial melting (Dai et al., 2018),incompatible element enrichments in the type II clinopyroxenecould be the result of element diffusion between clinopyrox-ene and infiltrating melts. This allows for the possibility ofconstraining the time of mantle metasomatism by the mineral

size, equilibrium temperature and diffusion rate (Brady andCherniak, 2010; Cherniak and Dimanov, 2010). The enrich-ments of quadrivalent Th in the core of type II clinopyroxenewith a radius of ~1000 mm were estimated to take >100 Ma(Fig. 5A). For high-valent elements (i.e., Nb and Ta), it will

155H.-K. Dai, J.-P. Zheng / Solid Earth Sciences 4 (2019) 150e158

take longer time to increase their contents in the clinopyroxenecore due to their lower diffusion rate (Cherniak and Dimanov,2010). Together with eruption age of the host basalts (~89 Ma,Dai et al., 2019), the metasomatism recorded by the type IIclinopyroxene should occur in the Paleozoic.

For the host basalts, the melting condition requires ~10%partial melting of a peridotite source or much higher meltingdegrees of pyroxenite source (Fig. 4B) because the latter tendsto have apparently low solidus temperature mantle pressure(Lambart et al., 2016). Considering the high contents ofincompatible element in these Mesozoic to Cenozoic basalts(Dai et al., 2019), such high melting degrees is suggestive of amantle source with highly enriched incompatible elements.Together with the overall unradiogenic SreNd isotopes, thissource should experience a relative short isolated ingrowth ofisotope systems (Stracke et al., 2003). Given the involvementof sediments in the basalt sources as suggested by the slightlydecoupled SreNd isotopes (Fig. 3C), the Pb isotopes of thesebasalts could be best approximated by the mixing of depletedmantle and altered oceanic crust with sediments of 0e500 Ma(Fig. 5B). In addition, the majority of regional ophiolite suitesthat represent the relicts of the Paleo-Asian Oceanic slab couldbe enveloped by the mixing between altered oceanic crust,depleted mantle and Paleozoic sediments.

6. Towards the subducted Paleo-Asian slab

The Phanerozoic oceanic slabs from three directions(Windley et al., 2010) are possible sources for the recycledoceanic crust materials in the mantle wedge beneath thenorthwest NCC. Though these slabs have overlapping isotopiccompositions (Dai et al., 2019), the following lines of evi-dence could favor the Paleo-Asian oceanic slab (>230 Ma,Yuan et al., 2016) as the source for the recognized recycledmaterials.

Firstly, the time of metasomatism recorded in the litho-spheric mantle (Fig. 5A) and the possible ages of the recycledsediments in the asthenosphere (Fig. 5B) are around ~200 Maor elder. Given the ages (� 92 Ma) of these basalts (Dai et al.,2019 and references therein), this could be roughly consistentwith the time of the Paleo-Asian ocean subduction (Xiao et al.,2015). Secondly, regional carbonatites of sediment precursorshave Sr isotopes comparable to those of the Paleozoic marinecarbonates (Chen et al., 2017) and the pyroxenites in thelithospheric mantle also have plenty of zircons with Paleozoicages (Liu et al., 2010), both of which are coeval with sub-duciton of the Paleo-Asian Ocean, thereby implying thepossible role of this subduction in the modification of theregional lithospheric mantle. In addition, the spatial compo-sitional variation of the Late Mesozoic to Cenozoic basaltsfrom the northwest NCC suggest that the availability of py-roxenites in the asthenosphere increase northward (Xu et al.,2017). Given a long residence time (e.g., >150 Ma) of thesubducted slabs in asthenosphere (Van der Voo et al., 1999;Wu et al., 2018), the northward increasing pyroxenite avail-ability is in accordance with the southward subduction of thePaleo-Asian ocean, during which the slab-derived melts

migated upwards and reacted with the ambient mantle peri-dotite to form the pyroxenites in the asthenosphere. Further-more, vigorous Paleozoic magmatism with arc affinity alongthe northwest margin of this craton suggests contributionsfrom the coeval subducted slab (Zhang et al., 2014). Finally,the northwest NCC are separated from the subduction from thesouth by the thick rigid Ordos block (Fig. 1A and B, Chenet al., 2014) and are far from the west-leading edge of thesubducted Pacific slab beneath the Trans-North Orogenic Belt(Liu et al., 2017). This spatial gap could eliminate remarkablecontributions from the subducted (Paleo-) Pacific slab to themodification of the mantle wedge beneath the northwest NCC,especially the metasomatism of the regional lithosphericmantle.

7. Conclusion

The mantle wedge beneath northwest North China Cratonwas modified to various degrees during the Paleozoic infil-tration of slab-derived melts. The availability of slab meltsdecreased from the slab-mantle contact to the uppermostmantle, leaving behind pyroxenites (reaction products at highmelt/rock ratio) in the asthenosphere and enrichments ofincompatible elements (reaction products at low melt-rockratio) in the lithospheric mantle. Conbined with the timeconstraints of this mass transfer, regional geological recordsand tectonic locality, the recycled materials in the mantlewedge was likely derived from the subduction of the Paleo-Asian Ocean in Paleozoic.

Acknowledgements

We thank the editor Dr. WD Sun for his invitation and thereviewers for their insightful and constructive suggestions andcomments. This work was supported by the projects from theNatural Science Foundation of China (41930215 and41520104003), the National Key R&D Program of China(2016YFC0600403), a scholarship under the state ScholarshipFund of China Scholarship Council (File No. 201706415070),a Macquarie University International Postgraduate Scholarship(iMQRES), and the Fund for Outstanding Doctoral Disserta-tion of CUG (Wuhan). This is publication 1387 from the ARCCentre of Excellence for Core to Crust Fluid Systems (http://www.ccfs.mq.edu.au) and 1334 in the GEMOC Key Centre(http://www.gemoc.mq.edu.au). This study is relevant toIGCP-662.

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