Geochemical characteristic of charnockite in North margin of ......LYS Charnockite), Guyang (BQG...

Running title: Geochemical characteristics of charnockites in North China Craton

Geochemical Characteristic of Charnockites in North Margin of

North China Craton: Indicating the Significiant of the Neoarchean

Tecnotic Event

SHI Qiang, FENG Fan, XU Zhongyuan

*, LIU Zhenghong, DONG Xiaojie and LI Gang

College of Earth Sciences, Jilin University, Changchun, China

Abstract:The Neoarchean charnockites of North margain of North China Craton (NCC) has become a hot topic

into understanding the Early Precambrian basement. Although there is a broad consensus that charnockite is

usually related to granulite facies metamorphism, whether its petrogenesis and tectonics characteristics still

remains controversial. Inclusions within hypersthene and garnet in charnockite are used to identify the peak

granulite facies mineral assemblage, with the formation of Magnesian–charnockite attributed to anatexis of the

protolith associated with this granulite facies metamorphism. The distribution of major and trace elements in

charnockite is very uneven, significant depleted in LILEs (eg. Cs, U, Th) and HFSEs (eg. Nb, Ta, P and Ti), riched

in Sr. Raising to the coexistence of Eu–enrichment and Eu–depletion type of REE patterns that influenced by the

content of plagioclase and the remnants minerals of zircon and apatite. Comparative the petrography, geochemistry

and geochronology data of Magnesian–charnockite indicate that the ratios of mafic pellites and basalts involved in

anatetic melting are different by the upwelling of mantle magma, also resulting in the Eu anormals characteristics.

The formation of the Magnesian–charnockite is closely connected with the subduction of the NCC oceanic crust

(About ~2.5Ga). However, Ferroan–charnockite may be the formed by the crystallization differentiation of the

upwelling of mantle–derived shoshonitic magma (About ~2.45Ga), with the lower crust material addition.

Keywords: Neoarchean, Magnesian–charnockite, Ferroan–charnockite, Metamorphic anatexis event, NCC

E-mail: [email protected].

1 Introduction

Charnockite has been considered as granitic rocks containing the orthopyroxene that formed under low water activity (or anhydrous) conditions by simulate phase equilibria of High–temperature and High–pressure (HTHP) melting experiments (Holland., 1900; Brown., 1994, 2004; Kriegsman., 2001; Le Maitre, 2002; Cheng et al., 2004). They are always discovered in precambrian high–grade metamorphic complex rocks. Recently years, Frost and Frost (2008) have redefined the charnockites as an orthopyroxene bearing granitic rocks of igneous rock origin or that are present as orthogneiss within a common constituent of granulite–facies metamorphic terrains or a metamorphic granulite facies of granite. They are usually showing spatial association of rocks of granulite. The origin and tectonic of the charnockites of NCC are remains debated, which has become a hot piont of the origin studies of the charnockites in Inner Mongolia (Wuchuan–Guyang charnockite), Hebei (Damiao charnockite), and Shandong (Yishui charnockite) provinces, China. The origin and tectonic has concluded as follow: (1) Production of migmatite formed by the anatexis of wall rock (Wang et al., 1984; Qian et al., 1985; Sun et al., 1989; Su et al., 2003; Zhang et al., 2014); (2) Formation of the protolith of tonalite–granodiorite, with the enviorment of the granulite facies metamorphism and involving the CO2–rich fluids (Geng et al., 1990); (3) Product of the crystallization differentiation (Wang et al., 1992); and (4) Partial melting of mafic crustal rocks (Ma et al., 2013a; Bai et al., 2015). The high–grade crustal of NCC, north margin of the between the Ordos Block and Yinshan Block, is characterized by anatectic charnockite and high–grade metamorphic complex. This anatectic charnockites mainly occurs in Shiguai–Baotou (Liu et al., 2017), Gonghudong–Guyang (Dong et al., 2012a; Ma et al., 2013a), XWLBL (Zhang et al., 2014; Shi et al., 2019a), Jining (Shi et al., 2019b, 2019c), Gehuyao (Zhang et al., 2017), Qian’an (Han et al., 2016) in Northern margin of NCC, and together with granulites, gneiss greenstone and khondalite belt, forming a significant component of the early precambrian metamorphic baseement (Fig.1). A lot of geochemistry and Isotope chronology bearing on anatectic charnockite from the early precambrian basement of NCC is compiled here. According to a study of the geochemical characteristics of the anatectic charnockite samples are least likely to have been influenced by the

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metamorphism superposited. However, most acheivements of the previously studies on charnockites are carried out from the aspects of metamorphism evolution and isotopic chronology. Rajesh et al.(2004) and Rajesh. (2012) attempted to study the petrogenesis and tectonic environment of charnockite by means of petrogeochemistry characteristics in South India. Basing on the previously Archean tectonic evolution models of NCC, the diference of geochemical characteristics of charnockite samples from different location{such as Shanheyuan (SHY) charnockite, Biqigou(BQG) charnockite, Cunkongshan(CKS) charnockite, Langyashan(LYS) charnockite, Xiwulanbulang(XWLBL) charnockite, Gehuyao (GHY) charnockite, Grhuyao(GHY) Hy–Tonalite} are used to constraint on the formation of the nature continental crust with time. In the process, we compiled geochemical data of these charnockites to discuss and develop an understanding of the geochemical characteristics might be related to their source rocks, petrogenetic processes and tectonic environments.

2 Geological Background

The Early Precambrian metamorphic basement of NCC is separated into the Eastern Block, Western Block and Paleoproterozoic Trans–North China Orogen (Zhao et al., 2005). Eastern Block (Fig. 1a) is composed of the Yinshan Block, Khondalite belt and Ordos Block, and at the end of the Paleoproterozoic, all of them has integrated into a centralized cratonic framework. It is well known that Yinshan block is the most largest and integrated area of early precambrian metamorphic in the western block, locating in NCC, with a ductile shear zone of south side bounded by the Xia Shihao–Jiu Guan ductile that output to East–West trending (Zhao et al., 1999, 2003, 2005). Yinshan Block is the largest and most complete area of Archean basement in the Western Block, located on the northern margin of the NCC, with the south side bounded by the Xia Shihao–Jiu Guan ductile east–west trending Xia–Shihao–Jiu–Guan ductile shear zone. Most of these basement rocks have characteristics of upper greenstone to lower–amphibolite facies metamorphism, and the metamorphic complex rocks also experienced high–grade metamorphism, generally of the high amphibolite to granulite facies (Jin et al., 1991,1994). The paleoproterozoic khondalite belt is located in the southern side of the Xiashihao– JiuGuan large–scale ductile shear zone (Fig. 1b). The upper part of the greenstone belt sequence comprises meta–komatiite and volcano–sedimentary rocks (Chen, 2007; Jian et al., 2012), granitic rocks from the upper Greenstone Belt is consists of TTG gneisses (Jian et al., 2005; Ren et al., 2010; Jian et al., 2012) and sanukite (Jian et al., 2012; Ma et al., 2013a). Occuring a dome structure consists of granulite and charnockite in the high–grade metamorphic complex rocks, it is also exposed mainly in the Baotou–Wuchuan–Guyang–Jining–Gehujiao area (Zhang et al., 2005; Ma et al., 2013a; Liu et al., 2017). Zircon dating of these rocks of the charnockites (XWLBL–JN Charnockite) and TTG gneisses (Wuchuan–Guyang–Siziwangqi area Gneisses) have affirmed that the metamorphic intrusive rocks from the North margian of NCC are more possibly formed in the Neoarchean (Dong et al., 2012a; Jian et al., 2012; Ma et al., 2013a; Zhang et al., 2014; Shi et al., 2019a). Previously study have shown that metamorphic origin zircon dating from the Greenstone belt, TTG and high–grade metamorphic complex obtained the metamorphic ages of 2.55–2.50 Ga (Jian et al.,2005, 2012; Ma et al., 2013a. 2013b; Wang et al., 2015; Liu et al., 2017; Chen et al., 2017). There are also some Neoarchean– Paleoproterozoic high–grade metamorphic complex rocks widely distributed in the khondalite series Belt and Yinshan Block, more and more studies have shown the metamorphic ages of ~2.5Ga and ~1.95Ga are widespread of the NCC (Jian et al.,2005, 2012; Ma et al., 2013a. 2013b; Wang et al., 2015; Liu et al., 2017; Guo et al., 2001; Wang et al., 2005; Wan et al., 2006, 2009, 2011, 2013a, 2013b, 2015; Santosh et al., 2006, 2007a, 2007b; Xu et al., 2011; Dong et al., 2013; Cai et al., 2014; Ma et al., 2015; Chen et al., 2017; Shi et al., 2018, 2019a, 2019b, 2019c).

Granulitic units are composed of granulite and high–grade metamorphic gneisses that have been retrogressed, both of which are closely associated with anatectic charnockite (Fig. 1c). Anatectic charnockite and gneisses are present in the NCC as irregularly shaped or banded units scattered throughout the localities of Jining Sanchakou (JN Charnockite), Baotou Shiguai (SHY Charnockite and LYS Charnockite), Guyang (BQG Charnockite and CKS Charnockite), Xiwulanbulang (XWLBL Charnockite), Datong Gehuyao (GHY Charnockite and GHY Hy–Tonalite), however, some charnockites might be related to mantle sources magmatic generates melting (Yang et al., 2014; Shi et al., 2019). The Neoarchean charnokite of Yinshan Block has been a hot topic into understanding the precambrian geology of the NCC. Although there is a broad consensus that the charnokite is usually related to granulite facies metamorphism, whether its petrogenesis and tectonics still remains controversial. Previous study have shown that the charnockite–granulite and other anatectic original rocks are closely distribution along to each other in spatially (Zhang et al., 2014; Shi et al., 2019a). We are also found that there are also two types hypersthene in NCC Charnockite (this paper): ①First type, with the characteristics of irregular in shape and xenomorphic structure, indicating a metamorphism origin. ②Second type, the hypersthene has the feature of tabular structure, without a obviously xenomorphic structure, refering to a magmatic origin. The purpose of our study is to contrast the


geochemical and geochronology of these rocks to the existing high–grade metamorphic rocks research achievements which collected from the nearby combination in order to better understand the evolution of the charnockites in the NCC. Comparing our results to those charnockite bodies reported in the Southern India where has a very mature understanding of the origin, material source of charnockite and revealing the contribution on regional tectonic evolution.

Fig.1 Sketch map showing distribution of late Archean terranes in the NCC (Modified after Zhao et al., 2005;

Dong et al., 2012a; Ma et al., 2013a; Zhang et al., 2014; Liu et al., 2017), in which the position of Fig. 1b is

indicated and published zircon ages (mostly SHRIMP and LA–ICP–MS) are compiled. Northern margin of the

NCC Yinshan Block metamorphic Dating Statistics (Fig. 1b, Compiled after Zhao et al., 1998, 1999; Zhang et al.,

2005; Tao and Hu, 2002; Jia et al., 2004; Jian et al., 2005; Ma et al., 2010). Detailed geological map of the

Xiwulanbulang area and Sampling locations (Fig.c).

3 Charnockite Petrography in NCC

The hypersthene(1–5%) of SHY Charnockite is irregular in shape and tabular structure, with partly hypersthene has a porphyritic texture. Biotite (1–5%) is fine flake, both of them are surrounding the hypersthene. Plagioclase (55–65%) has the characteristics of polysynthetic twins, with a irregular granular in shape, and it is also interstitial to hypersthene and biotite. Microcline (20–35%) always surrounds the hypersthene obviously. Quartz (15–20%) has a irregular serrated and resorbed grain boundaries characteristics, showing a granular texture and encircling the hypersthene (Fig.2b).

BQG Charnockite has a typical mineral assemblage of plagioclase (35–40%), microcline (15–20%), hypersthene (5–10%), biotite (5–10%) and quartz (15–20%). Hypersthene occur as subhedral short columns, with pyroxene chain, part of them retrograded to biotite. Showing a typical xenomorphic granular structure with quartz and plagioclase peritectic. Plagioclase displaying polycrystalline twins. Microcline has hypidiomorphic xenomorphic granular structure (Fig.2d).


The garnet (1–5%) of LYS Charnockite also has a typical xenomorphic granular structure, surrounded by hypersthene and irregular quartz. Hypersthene (1–5%) has irregular granular structure, usually symbiosis with iregular granular quartz, surrounded by the garnet. And showing xenomorphic structure with quartz and plagioclase peritectic. Plagioclase (30–40%) displaying polycrystalline twins characteristics. Microcline (15–20%) has hypidiomorphic–xenomorphic granular structure. The quartz (15–20%) has a granular texture characteristics, with an irregular serrated and resorbed grain boundaries. Hornblende (1–5%) has a iregular texture, aways surrounded by hypersthene (Fig.2f , 2h).

CKS Charnockite has a mineral assemblage of plagioclase (15–25%), microcline (45–55%), hypersthene (1–5%), biotite (1–5%) and quartz (15–30%). Hypersthene also has xenomorphic structure, with the quartz and plagioclase peritectic. Plagioclase also displaying polycrystalline twins. Microcline has hypidiomorphic or xenomorphic granular structure, encircling the plagioclase and quartz (Fig.2j).

The hypersthene (5–10%) of JN Charnockite has the xenomorphic structure with quartz and plagioclase peritectic, in which irregular in shape and has the tabular structure, occuring with granular quartz and partly hypersthene has a porphyritic texture (Fig.2l). Plagioclase (50–55%) is irregular in shape, with the polysynthetic twins . Microcline (15–25%) surrounds the hypersthene. Quartz (10–15%) has a irregular and serrated characteristics, usually encircling the hypersthene and feldspar (Fig.2l).

XWLBL Charnockite is composed of the mineral assemblage of hypersthene (5–10%), garnet (1–5%), plagioclase (35–40%), microcline (10–15%) and quartz (15–20%). Garnet has the feature of xenomorphic structure, surrounded by irregular quartz and hypersthene. Hypersthene has a feature of irregular granular in shape, occuring with the irregular granular quartz characteristics, and all of them are surrounding by the garnet (Fig.2f). Plagioclase has a irregular granular in shape, interstitialing to hypersthene and garnet. Microcline also surrounds the hypersthene (Fig.2f). Quartz has a feature of irregular serrated and resorbed grain boundaries, encircling the hypersthene and feldspar (Fig.2f ).

GHY Charnockite (Fig.2f) is composed of hypersthene (5–10%), hornblende (1–5%), plagioclase (40–55%), microcline (10–15%), quartz (5–20%). Hypersthene has xenomorphic structure with quartz and plagioclase peritectic, and it is also has a irregular granular structure usually symbiosis with iregular granular quartz, surrounding the hornblende (Fig.2n).

GHY Hy–Tonalite has piklblatileture characteristics, and it has mineral composed of irregular granular quartz (15–20%), hornblende (1–5%) and plagioclase (45–50%), with the irregular serrated and resorbed grain boundaries (Fig. 2p). Hypersthene (1–5%) has xenomorphic structure with quartz and plagioclase peritectic, and all of them are always surrounded by plagioclase, quartz and microcline (5–10%).

Figure.2 The contact between charnockite and granulite, Granulite inclusions in charnockite, the gradational

contact between charnockite and granulite, and part of granulite retrogressed to amphibolite of NCC Charnockite

(SHY Charnockite, BQG Charnockite, LYS Charnockite, CKS Charnockite, JN Charnockite, GHY Charnockite,

GHY Hy–Tonalite) in the field. (eg. 2a, 2c, 2e, 2k, 2m, 2o). Banded leucosome and melanosome in charnockite


(GHY Hy–Tonalite). (eg. b, d, f, h, j, l, n, p) Optical photomicrographs of charnockite (SHY Charnockite, BQG

Charnockite, LYS Charnockite, CKS Charnockite, JN Charnockite, GHY Charnockite, GHY Hy–Tonalite).

Abbreviations are as follows: Chn = charnockite; Grn = granulite; Fels = leucosomes; Hy = hypersthene;

Mi=Microcline; Pl = plagioclase; Q = Quartz; Opx = Orthopyroxene; Cpx = clinopyroxene; Hb = hornblende.

4 Analytical And Methods

The compositions of major–element of charnockite samples were tested on the Axios X–ray fluorescence spectrometer at the China National Research Center for Geoanalysis, Beijing, China. The trace–element analyses were measured on a Elan 9000 ICP–MS (Inductively Coupled Plasma–Mass Spectrometer), mading in the PerkinElmer company of United States in USA, and the accuracy of analysis is better than 10%. Geochemistry compositions and analytical standard samples for each major and trace element are given in Supplementary Supplementary Table 3. 5 Results 5.1 Effect of metamorphic superimposed

A detailed geochemical study of Nagercoil charnockites in southeastern India affected by the superimposed metamorphism of late Neoproterozoic–Precambrian granulite facies metamorphic is carried out (Rajesh et al., 2011, 2012). Considering the influence from the later metamorphic superimposed, a geochemical comparative study of low–Sr Nagercoil charnockite samples was made with that of the dehydration zones of the Opx (orthopyroxene) bearing metamorphic, occurring in gneisses from southern India and other areas (Fig. 3 and 4).They are also considered to represent in situ stages of granulite formation driven by the influx of low–aH2O fluids. According to the content of Sr of NCC charnockite can be divided into two types of High Sr (Fig 3, Sr: 518–911 ppm) and Low Sr (Fig 3, Sr: 143–416 ppm). Among them, high–Sr and low–Sr charnockites have a similar SiO2 content (60–74 wt.%), at the same SiO2 content condition, high–Sr anatetic charnockite is relatively enriched with Al2O3, K2O and Na2O, FeO

T, Rb, depleted in Nb (Fig 4). High–Sr anatetic charnockite has the

characteristics of trondhjemite–tonalite–granodiorite in An–Ab–Or diagram, however, most samples of low–Sr charnockite has the characteristics of tonalite–granodiorite–monzonitic granite (Fig 5). The characteristics of low–Sr charnockite with high K2O and Nb contents are closely related to previous geochemical studies. It is demonstrated that potassium plays an important role in the formation of some dehydrated metamorphic zones (Fig. 4c, 4d; Stahle et al., 1987; Raith and Srikantappa, 1993). It is also very similar to the characteristics of high–Sr charnockite in southern India studied by Rajesh et al (2011).

Figure 3. The charnockites of North margin of NCC SiO2 vs. Sr diagram. See Rajesh et al. (2011) for references

used to compile the compositional range of orthopyroxene–bearing metamorphic dehydration zones. Lower SiO2

content samples(<60 wt.%) are aimed for comparing with higher samples(>60 wt.%) in the Fig.3, 4, 6, 8, 9, 11a,

12a, 16a, however, they are removed in Fig.5, 7, 10, 11b, 12b, 13, 14, 15, 16b, 17.

Geochemical characteristics indicate that low–Sr charnockite may be related to later metamorphism,

whereas high–Sr charnockite were most likely not affected by late metamorphism. The results of geochronology show that the charnockites in the early Precambrian basement are widely affected by the post–metamorphism, and The study results of the geochronology show that the charnockites in the early Precambrian basement are widely affected by the post–metamorphism, and it is related to the regional metamorphism of the northern margin of the NCC at ~2.45Ga , ~1.95 and ~1.85 (Li et al.,


2000; Zhao et al, 2005; Dong et al., 2007; Jian et al., 2008; Wan et al., 2008; Li et al, 2011; Jian et al., 2012; Ma et al., 2013a; Ma et al., 2013b; Ma et al., 2013c; Guo et al, 2012; Liu et al., 2013; Cai et al., 2014; Bai et al., 2015; Xu et al., 2015; Ma et al., 2016; Yang et al., 2016; Shi et al., 2018). Therefore, we selected high Sr samples for corresponding study.

Figure.4 The Hark diagram of North margin of NCC high–Sr and low–Sr charnockites. Amphibolite dehydration

melts (only those with comparable P–T conditions to the Nagercoil charnockites are plotted) from Beard &

Lofgren (1991) and Rapp & Watson (1995), and high–temperature hydrous basalt melts from Sisson et al. (2005)

are shown for comparison. The compositional range of dehydration zones (metamorphic incipient charnockites) in

gneisses from southern India and elsewhere are from Janardhan et al.(1982), Hansen et al. (1987), Yoshida et al.

(1991), Dobmeier & Raith (2002), Harlov et al. (2012). For clarity, garnet–bearing and garnet–absent charnockites

are not distinguished.

Figure.5 The An–Ab–Or diagram of North margin of NCC high–Sr and low–Sr charnockites.

5.2 Geochemical characteristics of charnockites

Comparison and analysis of geochemical data of charnockites from different locations of the world, such as the Magnesian–charnockite has the calcic to calc–alkalic and metaluminous group characteristics; However, the Ferroan–charnockite has the feature of alkali–calcic to alkalic and metaluminous group, and also having a transitional group that straddles from ferroan to magnesian group (Rajesh and Santosh, 2004; Frost and Frost, 2008; Rajesh, 2012). Genaraly speaking, Ferroan–charnockite is more likely occured in an extensional tectonic environment (Frost and Frost, 2008; Rajesh, 2012; Rajesh and Santosh, 2012), however, the Magnesian–charnockite is more possibly occured in a magmatic arc setting (Emslie, 1991; Frost et al., 2001; Keppie et al., 2003; Rajesh et al., 2011). The geochemical characteristics of charnockite in different areas of the northern margin of the NCC are roughly similar, but they still have own unique characteristics. The magmatism of charnockite of older can only consider high Sr samples which have not been affected by metamorphism superimposed. According to the characteristics of rare earth element Eu anomaly characteristics, high Sr samples of charnockite can be divided into two types: Eu enrichment and Eu depletion. The ratio of


A/CNK is 0.52–1.24, with metaluminous to weak peraluminium characteristics (Fig.11).

Figure.6 The SiO2 vs.FeOT/(FeOT+MgO) diagram of Eu enrichment type and Eu depletion type charnockite

samples from the north margin of NCC (Frost, 2001; Rajesh, 2012; Rajesh and Santosh, 2012). The legend is the

same as Figure 3.

SHY Charnockite mainly located in the north margin of NCC, South of the Shiguai and near Shanheyuan area (Fig.1b, Sample Number from SHY–1 to SHY–9 ), and most of the samples have magnesian charnokite characteristics (Fig.6, FeO

T/(FeO

T+MgO): 0.64–0.96), prossesing a partition

curve of Eu–enrichment type (Table 1, Eu/Eu*:1.07–3.18, FeOT/(FeO

T+MgO): 0.80–0.96, Magnesian

charnokitess) and Eu–depletion type (Table 1, Eu/Eu*: 0.35–0.95, FeOT/(FeO

T+MgO): 0.64–0.77,

Ferroan charnokitess) obviously. The An–Ab–Or diagram shows that the Eu enrichment type has the characteristics of granodiorite–monzogranite, and the Eu depletion type has granite characteristics (Fig.7). Compering with Eu–depletion type, Eu–enrichment type samples are relatively enriched in Al2O3, MgO, CaO, P2O5, and depleted in FeO

T, Na2O, K2O, Na2O, Nb, Rb (Fig.8). Eu enrichment type

samples has the characteristic of the Calclic to Calclic–Alkline series, Eu–depletion type samples has Calclic–Alkline to Alkline–Calclic, all of them have potassium characteristics. The total REE content is relatively high in samples with low Eu/Eu* values (Fig.10b, Table 1; Eu enrichment type ∑REE: 54.24–160.03ppm; Eu–depletion type ∑REE: 149.10–370.76 ppm), and all of them has the characteristic of HREE depletion obviously. The total content of trace elements is very similarity (Fig.10a), all of them enrichment in LILEs (eg. K, Rb, Ba), depleted in HFSEs (eg. Nb, Ta, P and Ti). Specially, the Eu–enrichment type samples riched in HPEs (eg. Th), more depleted in LILE (eg. Rb and Ba), and more depleted in partial HFSEs (eg.Ti). The ratio of A/CNK is 0.87–1.10, with the characteristic of metaluminous to weak peraluminium (Fig.11b).

Figure.7 The An–Ab–Or diagram of Eu enrichment type and Eu depletion type charnockites samples from the

north margin of NCC (O’Connor., 1965). Solid lines represent Eu enrichment type samples, dotted line represent

Eu enrichment type samples.

BQG Charnockite mainly located in the north margin of NCC, North–West of the Baotou and near

Biqigou area (Fig.1b, Sample Number from BQG–1 to BQG–10), and the samples have magnesian charnokites characteristics (Fig.6; FeO

T/(FeO

T+MgO): 0.66–0.76), prossesing a partition curve of

Eu–depleted type. The An–Ab–Or diagram shows that the Eu–depletion type has granite–monzonitic granite characteristics. Compering with other Eu–enrichment type charnockites, Eu–depletion type


samples are relatively depleted in Al2O3, CaO, Na2O, and enriched in FeOT, MgO, K2O, P2O5,TiO2, Nb,

Rb (Fig.8). Eu–enrichment type samples has the characteristic of the Calclic–Alkline to Alkline series. The total REE content is relatively high in samples with low Eu/Eu* values, Eu–depleted type (Fig.10d, ∑REE: 104.93–481.31 ppm), and all of them has the characteristic of LREE enrichment and HREE depletion obviously. About the trace elements (Fig.10c), similar to other Eu–depletion type samples, all of them more enrichment in LILEs (eg. K, Rb, Ba), and depleted in HFSEs (eg. Nb, Ta, P and Ti), and more depleted in partial HFSEs (eg. Ti). The ratio of A/CNK is 0.87–1.08, with the characteristic of metaluminous to weak peraluminium (Fig.11b).

Figure.8 The Hark diagram of Eu–enrichment type and Eu–depletion type charnockite samples from the north

margin of NCC

GHJ Charnockite mainly located in the north margin of NCC, North–east of the Datong and near Gehuyao area (Fig.1c, Sample Number from GHY–1 to GHY–26), and most of the samples have magnesian charnokites characteristics (Fig.6, FeO

T/FeO

T+MgO: 0.38–0.68), prossesing a partition

curve of Eu–enrichment type (Table 1, δEu: 1.05–4.34, FeOT/(FeO

T+MgO): 0.58–0.68) and

Eu–depletion type (Table 1, δEu: 0.90–1.02, FeOT/(FeO

T+MgO): 0.39–0.68). The An–Ab–Or diagram

shows that the Eu–enrichment type has the characteristics of granodiorite–tonalite, and the Eu–depletion type has trondhjemite–granodiorite–tonalite characteristics. Compering with Eu–depletion type, Eu–enrichment type samples are relatively enriched in Al2O3, Na2O, CaO, Ba, Rb, and depleted in FeO

T, MgO, K2O, Nb (Fig.8). Eu enrichment type samples has the characteristic of the

Calclic to Calclic–Alkline , Eu–depletion type samples has Calclic–Alkline to Alkline–Calclic. The total REE content is relatively high in samples with low Eu/Eu* values (Fig.10f, Eu–enrichment type


∑REE: 35.60–146.40 ppm; Eu–depletion type ∑REE: 126.7–246.0ppm), all of them has the characteristic of HREE depletion obviously. The total content of trace elements is very similarity (Fig.10e), all of them enrichment in LILEs (eg. K, Rb, Ba), depleted in HFSEs (eg. Nb, Ta, P and Ti). Specially, the Eu–enrichment type sample (Fig. 10e) enriched in HPEs (eg. Th), depleted in partial LILE (eg. Rb and Ba), and more depleted in partial HFSEs (eg. Ti). The ratio of A/CNK is 0.87–1.10, with the characteristic of metaluminous to peraluminous (Fig.11b).

Figure.9 The diagram of the SiO2 vs. (Na2O+K2O–CaO)(wt.%) Eu–enrichment type and Eu–depletion type

charnockite samples from the north margin of NCC (Frost et al.,2001)

LYS charnockite mainly located in the north margin of NCC, South–east of the Baotou and near

Shiguai area (Fig.1b, Sample Number from LYS–1 to LYS–12), and most of the samples have Magnesian–charnokite characteristics (Fig.6, FeO

T/FeO


curve of Eu–enrichment (Fig.10h, Table 1, δEu: 1.04–4.39, FeOT/ (FeO

T+MgO): 0.41–0.70) and

Eu–depletion type (Fig.10h, Table 1, δEu: 0.57–0.94, FeOT/(FeO

T+MgO): 0.56–0.67). The An–Ab–Or

diagram shown that the Eu–enrichment type has the characteristics of granodiorite–tonalite, the Eu–depletion type has trondhjemite–granodiorite–tonalite characteristics (Fig.7). Compering with other Eu–enrichment type charnockites, Eu–depletion type samples are relatively depleted in Al2O3, Na2O, CaO, Ba, Rb, and enriched in FeO

T, MgO, K2O, Nb (Fig.8). Eu–enrichment type samples has the

characteristic of the Calclic series, Eu–depletion type samples has Calclic to Alkline–Calclic. The content of total REE is relatively high in samples with low Eu/Eu* values (Fig.10h, Eu–enrichment type ∑REE: 39.91–99.8 ppm; Eu–depletion type ∑REE: 77.19–109.18ppm), and all of them has the characteristic of HREE depletion obviously. About the trace elements (Fig.10g), the total content of Eu–enrichment and Eu–depletion type are very similarity, all of them enrichment in LILEs (eg. K, Rb, Ba), depleted in HFSEs (eg. Nb, Ta, P and Ti). Specially, the Eu–enrichment type (Fig 10g) sample enriched in HPEs (eg.Th), more depleted in partial LILEs (eg. Rb and Ba) and HFSEs (eg.Ti). The ratio


of A/CNK is 0.70–1.06, with the characteristic of metaluminous to weak peraluminium (Fig.11b).

Figure.10 The diagram of the primitive mantle–normalized trace element spidergrams (Left) and the

Chondrite–normalized REE patterns (Right) (Normalization values after Sun and McDonough, 1989) in Eu

enrichment type and Eu depletion type charnockites samples from the north margin of NCC (Data from Chacko et

al.,1992; Beard et al., 1994).

CKS Charnockite mainly located in the north margin of NCC, west of the Baotou and near

Cunkongshan area (Fig.1c, Sample number from CKS–1 to CKS–15), most of the samples have Magnesian–charnockite characteristics (Fig.6, FeO

T/FeO


curve of Eu–enrichment type (Fig.10j, δEu: 1.24–4.41, FeOT/(FeO

T+MgO): 0.55–0.74) and

Eu–depletion type (Fig.10j, δEu: 0.92–1.0, FeOT/(FeO

T+MgO): 0.51–0.68). The An–Ab–Or diagram

shows that the Eu–enrichment type has the characteristics of trondhjemite–granodiorite–tonalite, and the Eu–depletion type has granodiorite–tonalite characteristics (Fig.7). Compering with other


Eu–enrichment type charnockite, Eu depletion type samples are relatively depleted in FeOT, MgO, K2O,

Nb, and enriched in Al2O3, Na2O, CaO, Ba, Rb (Fig.8). Eu–enrichment type samples has the characteristic of the Calclic series, Eu–depletion type sample has Calclic to Alkline–Calclic. The total REE content is relatively high in samples with low Eu/Eu* values (Fig. 10J, Eu–enrichment type ∑REE: 56.83–112.65 ppm; Eu–depletion type ∑REE: 107.56–168.18 ppm), and all of them has the characteristic of HREE depletion obviously. About the trace elements (Fig 10i), the total content of Eu enrichment and Eu depletion type are very similarity, all of them enrichment in LILEs (eg. K, Rb, Ba), and depleted in HFSEs (eg. Nb, Ta, P and Ti). Specially, the Eu–enrichment type sample (Fig 10i) enriched in HPEs (eg.Th), more depleted in partial LILE (eg. Rb and Ba) and partial HFSEs (eg. P and Ti). The ratio of A/CNK is 0.76–1.08, with the characteristic of metaluminous to weak peraluminium (Fig.11b).

JN Charnockite mainly located in the north margin of NCC, Jining area (Fig.1b, Sample Number from JN–1 to JN–10), most of the samples have Ferroan–charnockite characteristics (Fig.6, FeO

T/FeO

T+MgO: 0.69–0.93), prossesing a partition curve of Eu–enrichment type (Fig.10l, δEu:

1.07–1.90, FeOT/ (FeO

T+MgO): 0.73–0.93) and Eu–depletion type (Fig. 10l, δEu: 0.49–0.94,

FeOT/(FeO

T+MgO): 0.69–0.77). The An–Ab–Or diagram shows that the Eu–enrichment type has the

characteristics of granodiorite–tonalite, and the Eu–depletion type has granodiorite–tonalite characteristics (Fig.7). Compering with other Eu–enrichment type charnockite, Eu depletion type samples are relatively depleted in Al2O3, K2O, Ba, Rb, and enriched in FeO

T, MgO, Na2O, CaO, P2O5,

TiO2, Nb (Fig.8). The Eu–enrichment type samples has the characteristic of the Calclic series, Eu–depletion type samples has Calclic to Calclic–Alkline. The total REE content is relatively high in samples with low Eu/Eu* values (Fig 10l, Eu enrichment type ∑REE: 135.52–372.49 ppm; Eu depletion type ∑REE: 236.35–389.50ppm), and all of them has the characteristic of HREE depletion obviously. About the trace elements (Fig.10k), the total content of Eu–enrichment and Eu depletion type are very similarity, all of them enriched in LILEs (eg. K, Rb, Ba), and depleted in HFSEs (eg. Nb, Ta, Nd, P and Ti). Specially, the Eu–enrichment type sample (Fig.10k) enriched in HFSEs (eg. Th), more depleted in LILEs (eg. K, Rb and Ba) and partial HFSEs (eg. Ta, P and Ti). The ratio of A/CNK is 0.84–1.02, with the characteristic of metaluminous to weak peraluminium (Fig.11b).

GHY Hy–Tonalites mainly located in the north margin of NCC, North–east of the Datong and near Gehuyao area (Fig.1c, Sample Number from GHYH–1 to GHYH–10), most of the samples have Magnesian–charnokitesss characteristics (Fig.6, FeO

T/FeO

T+MgO: 0.62–0.87), and prossesing a

partition curve of Eu–enrichment type (Fig.10n, δEu: 1.07–1.90; FeOT/(FeO

T+MgO): 0.73–0.93). The

An–Ab–Or diagram shows that the Eu–enrichment type has the characteristics of trondhjemite– granodiorite–tonalite (Fig.7). Compering with other charnockites in NCC, Eu–depletion type samples are relatively enriched in Al2O3, CaO, Na2O, and depleted in FeO

T, MgO, K2O, P2O5, TiO2, Nb, Rb

(Fig.8). Samples have the feature of Calclic to Alkline–Calclic series, The total REE content is relatively low in samples (∑REE: 31.6–149 ppm ), and all of them has the characteristic of HREE–depletion obviously. About trace elements (Fig.10m), the total content of Eu–enrichment type samples, and all of them enrichment in LILE (eg. K, Rb and Ba), more depleted in HFSEs (eg. Nb, Ta, Nd, P and Ti). The ratio of A/CNK is 0.97–1.11, with the characteristic of metaluminous to peraluminium (Fig.11b).

Figure.11 The diagram of the SiO2 vs. A/KNC (after Rajesh et al., 2011) (a) and the A/KNC vs. A/NK (Frost et al.,

2001) (b) in Eu–enrichment type and Eu–depletion type charnockite samples from the north margin from

NCC{The legend is the same as Figure 8}.

XWLBL Charnockite mainly located in the north margin of NCC, west of the Wuchuan and near Xiwulanbulang (Fig.1b), most of the samples have Magnesian–charnockite characteristics (Fig.6, FeO

T/FeO

T+MgO: 0.56–0.72), prossesing a partition curve of Eu–enrichment type (Fig.10p, δEu:


1.24–3.62; FeOT/(FeO

T+MgO): 0.63–0.72) and Eu–depletion type (Fig. 10p, δEu: 0.60–0.96;

FeOT/(FeO

T+MgO): 0.56–0.71). The An–Ab–Or diagram shows that the Eu–enrichment type has the

characteristics of trondhjemite–granodiorite–tonalite, and the Eu–depletion type has granodiorite– tonalite characteristics (Fig.7). Compering with other Eu–depletion type charnockites, Eu–enrichment type samples are relatively depleted in FeO

T, MgO, K2O, Na2O, CaO, P2O5, TiO2, Nb, and enriched in

Al2O3, Ba, Rb (Fig.8). Eu–enrichment type sample has the characteristic of the Calclic series, Eu–depletion type sample has Calclic to Calclic–Alkline characteristics. The content of total REE is relatively high in samples with low Eu/Eu* values (Fig. 10p, Eu–enrichment type ∑REE: 40.68–56.23 ppm; Eu–depletion type ∑REE: 75.24–220.29 ppm), and all of them has the characteristic of HREE– depletion obviously. The total trace elements content of Eu–enrichment and Eu–depletion type sample is very similarity, all of them enriched in LILEs (eg. K, Rb, Ba), depleted in HFSEs (eg. Nb, Ta, Nd, P and Ti). Specially, the Eu–enrichment type sample (Fig.10o) enriched in HPEs (eg.Th), more depleted in partial LILEs (eg. Rb and Ba) and HFSEs (eg. Ta, P, Nb and Ti). The ratio of A/CNK is 0.74–1.04, with the characteristic of metaluminous to weak peraluminium (Fig.11b).

6 Discussions 6.1 Petrogenesis and sources rock

Shi et al. (2019b) studies shown that JN Charnockite has a typical characteristics of anatetic structure, such as the exists universally of sieve texture in garnets that the mineral assemblages of the peak stage of granulite facies metamorphism (Pl+Cpx+Hb+Qtz) are retained. Ma et al.(2013a), Zhang et al.(2014), Shi et al. (2019a) refer to XWLBL Charnockite has the typical characteristics of meta–anatetic mineral. And the similarity typical anatetic structure in SHY Charnockite, with the granulite facies metamorphism mineral assemblages of Pl+Hy+Di+Hb+Qtz (Xu et al., 2015). In this study, the characteristic of anatetic charnockites are closely symbiosis with the basic–felsic granulite (Wulashan–Xinghe group) in space, and the leucosome felsic zone and dark granulite xenoliths development, indicating the anatetic melting occur migration and differentiation (Fig.2a, 2c, 2e, 2g, 2i, 2k, 2m, 2o). In general, the hypersthene in anatetic characteristics charnockite (Magnesian–charnockite) has a xenomorphic structure and irregular in shape, associating with plagioclase accumulation. The characteristics of plagioclase and quartz peritectic in the crystal show that hypersthene is a typical metamorphism genetic. The hypersthene in magmatic genetic characteristics charnockite (Ferroan–charnockite) has the characteristics of tabular structure, and it does not has the sieve texture, with a typical magmatic genetic characteristics. We noticed that the typical granulite facies metamorphism mineral assemblages (Pl+Cpx+Hb+Qtz) which has the characteristics of typicaly erosion structures, with a harbour–like structure and some of them have residual amphibole and biotite in anatetic charnockites (SHY Eu–enrichment type Charnockite, CKS Charnockite, LYS Charnockite, BQG Charnockite, XWLBL Charnockite, JN Eu–enrichment type Charnockite, GHY Charnockite, GHY Hy–Tonalites; Hereinafter refered to as ‘Anatetic charnockites’), and all of these phenomena indicate the formation of metamorphism–anatetic charnockites (Fig.2b, 2d, 2f, 2h, 2j, 2l, 2n, 2p). The residual mineral phases of pyroxene and garnet have generally sieve texture (Fig. 2d, 2f, 2h, 2l, 2p), with melting corrosion structure of Pl+Hb+Qtz mineral assemblages, and raising to a mineral assemblages of granulite facies metamorphism of the stage of prograde metamorphism (Lu et al ., 1992, 1993; Shi et al., 2019b). Previosly study of traditional calculation of temperature and pressure may suggest that isothermal decompression after peak metamorphism was intimately related to the formation of anatetic charnockites (Shi et al., 2018; Shi et al., 2019a), in which consistent with the anatetic characteristics charnockites in this paper.


Figure.12 The diagram of the SiO2 vs. K2O (Peccerillo and Taylor., 1976) (a) and the K vs. Na vs. Ca (Barker and

Arth., 1976) (b) in Eu–enrichment type and Eu–depletion type charnockite samples from the north margin from

NCC{The legend is the same as Figure 8}.

The coexistence of Eu–enrichment and Eu–depletion type charnockites are prossesing a partition curve of Eu–enrichment type considered to be a typical feature of NCC anatetic granite, considered as a typical anatetic feature (Song et al., 2005; Ma et al., 2015; Shi et al., 2018), related to the redistribution of elements in the process of anatexis. Eu anomaly become the most obviously difference to the charnockites in southern India (Stuckless et al., 1989). The partition curve of Eu–enriched and Eu–depleted of the anatetic characteristic granite in the filed (SHY Eu–enrichment type Ccharnockite, GHY Charnockite, BQG Charnockite, LYS Charnockite, CKS Charnockite, GHY Hy–Tonalite, XWLBL Charnockite, JN Eu–enrichment type Charnockite), relatively enriched in LILEs (eg. K, Rb, Ba). It is also suggested that they are readily partition into the meltting and may be a small amount of fluid during the anatexis, and more depleted in HFSEs. These differences compositions of the trace–element may be reflected by the redistribution of chemical components during the anatexis. The characteristics of radiogenic elements (eg. Th and U) depletion can further support to an anatetic origin.

Previously experiment study indicated that the partial melting of continental crustal material, with the refractory residual REE enriched mineral of zircon and apatite which reduction of REE content in anatetic products (Gordon et al., 2013). The geochemical characteristics of anatetic charnockites are obviously depleted in the content of “P” that mainly related to the mineral of apatite. Hidaka et al (2002) study indicated that the Eu anomaly is closely related to the melanocratic mineral of plagioclase, hypersthene and garnet, raisesing a explanation for Eu–enrichment and Eu–depletion type anatetic charnockites. Comparing with Eu–enrichment type sample, Eu–depletion type sample has a relatively lower content of CaO and CaO+Na2O, however, the content of FeO

T, MgO, Nb, Ta, Zr, Hf, U, Th

relatively higher (Fig.8 and 10), and a lower content of Sr (Table 1). All of the characteristic of Eu–depletion samples has a higher content of melanocratic mineral and a lower content of plagioclase. The total amount of REE in Eu–enrichment samples is generally lower, and in some samples even 4–6 times lower than that in Eu–depletion samples (Table 1). We consider that the higher content of plagioclase and lower content of melanocratic mineral in NCC charnockites that further explained the primary separation of residual minerals of pyroxene (One of the mainly restricting factors of REE content of continental crust rocks) and new leucosome during the crystallization process. The REE characteristics of charnockites may be influenced by the refractory residual minerals such as zircon and apatite.

Figure.13 The diagram of the Y vs. Sr/Y in Eu–enrichment type and Eu–depletion type charnockite samples from

the north margin from NCC (Drummond and Defant.,1990)

We can observed a obviously depletion characteristics of HREE relative to LREE in the charnockite samples [(La/Yb)N =4.0–77.4] possible indicated that the presence of residual garnet in the source region of these charnockites since HREE can be strongly fractionated into garnet in consisten with the study by Johnson.(1998). However, there are also possessed a high ratio of the (La/Yb)N from the


sources rocks. Nagasawa (1970) study raised to the zircon may be cause to a strongly partition HREE over LREE, therefore, the fractionation of zircon may also cause to the HREE–depletion that we observed in this paper charnockites. And the characteristics of slight Zr depletion samples indicated that the zircon as a fractionating phase only plays a minor importance part of the charnockites in this paper. However, the feature of Zr enrichment in these charnockite samples may raise to accumulation of the zircon during its magmatic crystallization history. In this paper, we considered that the combined action of the residues of residual minerals such as apatite may lead to a sharp decrease in the total REE content of charnockite. In general, the geochemical characteristics of the anatetic charnockites in this region are as follows: the distribution of major and trace elements is extremely uneven, with the depletion of LILES (eg. Cs) and HFSEs (eg. U and Th) obviously, relatively more enriched in Sr and depleted in HFSEs (eg. Nb, Ta, P and Ti). Prossesing a unique REE partition curve of Eu enrichment and Eu depletion that not only the mainly particular characteristics of charnockites in this region. And the anatetic granite shows a similar characteristic in the Baotou and Jining area (Song et al., 2005; Ma et al., 2015; Shi et al., 2018). We confirmed that some variability and inheritance of geochemical characteristics of the charnockits, the former may be related to the subsequent convergence and migration of anatetic melting and the latter may be related to the source rocks.

Figure.14 The diagram of the Rb vs. Sr vs. Ba in Eu–enrichment type and Eu–depletion type charnockite samples

from the north margin from NCC after Rajesh and Santoshi (2004)

The various geochemical characteristics of charnockites can usually indicate the tectonic background of formation. Frost and Frost (2008) summarized the major geochemical characteristics of the formation of charnockites in different tectonic settings: ①Rift–related charnockite has the characteristics of ferroan alkali–calcic to alkalic metaluminous, as the component rocks of Anorthosite–Mangerite–Charnockite–Granite suite (Emslie, 1991). ②Delamination–related granites has the characteristics of small–volume, alkali–calcic to alkalic and magnesian plutons that connected with the delamination of thickened continental crust after a collision orogeny event. ③Deeply crustal partial melting related granite has the characteristics of the upwelling of hot ferroan magma, the compositions of geochemistry and isotopic indicated the crustal component has been involved (Young et al., 1997; Battacharya and Sen, 2000; Kar, 2003; Percival et al., 2003). ④Deeply eroded has the characteristics of alkali–calcic to alkalic and metaluminous granitoid chemistry plutons, indicating a deeply eroded magmatic arc tectonic settings. Ferroan–charnockite in the northern margin of NCC is different from the Damiao ~1.95Ga Ferroan–charnockite in Hebei Province (FeO

T/(FeO

T+MgO): 0.9–1.0, #Mg: 6–28)

in this paper (Yang et al., 2014), Jining and Shanheyuan Ferroan–charnockite (JN Eu–depletion type and SHY Eu–depletion type Charnockites, Hereinafter refered to as ‘Ferroan–charnockite’) has weak ferroan characteristics (Table 1, FeO

T/ (FeO

T+MgO): 0.84–0.96, #Mg: 7–37) Eu–enrichment type

sample has the characteristic of Calclic to Calclic–Alkline, Eu–depletion type has the characteristic of


Calclic–Alkline to Alkline–Calclic. Magnesian–charnockite (SHY and JN Eu–enrichment type Charnockite, CKS Charnockite, BQG Charnockite, LYS Charnockite, XWLBL Charnockite, GHY Charnockite, GHY Py–Tonalite, Hereinafter refered to as ‘Magnesian–charnockite’) are classified into Eu–enrichment type (Calclic to Calclic–Alkline characteristics) and Eu depletion type (Alkline–Calclic to Alkline characteristics). Above mentioned charnockites are consistent with the evolution of island arc magma along a calc–alkaline trend (Fig.12b, Magnesian and Ferroan charnockite characteristic, Calclic to Calclic–Alkline to Alkline), and all of them inconsistent with the Rift–related and Delamination–related granite. Comparing with the geochemistry characteristic of closely spatially granulite (Fig.1, Fig.2), and the characteristic of crustal sources of Nb–depletion (Fig.10), with the typical characteristic of plutonic rock. We consider that charnockites are related to the partial melting of lower crustal and island arc magma plutonic rock, they are associated with the granulite facies metamorphic. Eu–enrichment type charnockites shown a genetic relationship with TTG gneiss, and Eu–depletion type sample has an island arc magmatic magma characteristic (Fig.13).

The southern India and other different parts of the world obtained the compilations of geochemical data from charnockites, indicating the mostly Magnesian–charnockite belong to tonalitic rocks (trondhjemitic rocks are more likely to magnesian, but occurrences rarely related to the tonalitie rocks), whereas the Ferroan–charnockites are more likely to granodioritic–granitic rocks (Rajesh, 2007). In general, Frost and Frost., (2008) study refer to the Ferroan–charnockites are more likely occured in an extensional tectonic enviorment whereas Magnesian–charnockites more likely formed in an magmatic arcs setting (Rajesh, 2007). Similar to the southern India charnockites, JN Eu–depletion type and SHY Eu–depletion type Charnockites (Ferroan–charnockite) mainly belong to monzogranite–granite characteristics, however, anatetic charnockites (Magnesian–charnockite) has the granodiorite–tonalite characteristics. And all of them has the trend of calc–alkaline magma evolution of island arc (Fig.12b).

Charnockite is characterized by high Ba–Sr in this paper. Previously study raised to almostly all of the genetic mechanisms proposed for the high Ba–Sr charnockite formation require the lithospheric mantle material addition, such as (1) Qian et al., (2003) studies consider that high Ba–Sr granite derived from the melting of subcontinential lithospheric mantle; (2) Fowler (2001) refer to the Ba–Sr granite may be a production of crystal fractionation of associated shoshonitic magma derived from an enriched lithospheric mantle; (3) Shi et al., (2018, 2019a) studies indicated that high Ba–Sr anatetic granite related to the underplating of Sr– and Ba–rich mafic magma; (4) Ye et al., (2008) raise a point of view about high Ba–Sr granite is the products of partial melting of lower crust with a minor involvement of enriched mantle derived magma. Qian et al.,(2003) refer to the melt of continental lithospheric mantle generally forms potassic magmas (K2O+Na2O>5wt.%, TiO2<1.3wt.%, Al2O3: 14–19wt.%), however, the charnockite has the trend of calc–alkaline magma evolution of island arc in this paper (Fig. 12b), with a small part of samples have the characteristics of potassic. It is consider that more alkaline (K2O+Na2O>5wt.%) and enriched in K2O (K2O/Na2O>0.7) of crystal fractionation of shoshonitic magma generates melt, which is inconsistent with the K2O content of the charnockites in this paper. The depleted in Nb and Ti characteristic, which together are consistent with a continental crustal origin distinct from single mantle–derived magma. However, the difference of the degree of Nb–depletion raised to the problem of the charnockite formation. The isotope geochemistry of XWLBL High–Ba and Sr charnockite indicated that consistent with an underplating of Sr– and Ba–riched mafic magma during the process of the anatexis (Ma et al., 2013a; Zhang et al., 2014; Shi et al., 2018). Similar to the geochemistry of XWLBL Charnockite, anatetic charnockites transitional to source rocks in spatial (Shi et al., 2018, 2019a), and has a characteristic of High–Mg content (Table1, #Mg>45), in which indicated more mafic sources than basalt. Combined with the low content of Nb (<10ppm) elements and the value of εHf > 0 in most samples (In Table 2), mainly derived from juvenile crustal material and the addition of high Sr–Ba ingredient from the mantle. Therefore, the single source of mantle–derived magma is not credible. However, high Ba–Sr and Eu–depletion type charnockite studies of Jining area raise to petrogenesis of crystal fractionation of associated shoshonitic magma, while the Eu–enrichment type charnockite addition of high Sr–Ba ingredient from the mantle during the anatexis (Shi et al., 2019a). The geochemistry of SHY Eu–depletion Charnockite is similar to Jining Eu–depletion Charnockite, the values of εHf is –9.74~ +3.56 (In Table 2, Liu et al., 2017), and all of them has the low Mg content characteristic (#Mg<45), indicating the more basalt sources than mafic. At the same time, the content of Nb relatively higher (Nb > 15ppm) than anatetic charnockite (Average content of Nb:10ppm) that raising to a few of crustal material sources, and the geochemistry characteristics of K, Na content is consistent with crystal fractionation of associated shoshonitic magma. However, the crystal fractionation usually with the Eu–depletion characteristic (Ye et al., 2008), similar to JN Eu–depletion charnockites, we consider that SHY Eu–depletion Charnockite has the original of crystal fractionation associated with shoshonitic magma. Similar to the XWLBL charnockite, SHY Eu–enrichment type and JN Eu–enrichment type Charnockites are more likely related to the anatexis of the juvenile lower crustal.

For anatetic granite rocks, Drummond and Defant. (l990) refers to the depleted in Y and HREE, with a higher ratio of Sr/Y and La/Yb posibility formation by hornblende, clinopyxene and garnet in residual


phases after partial melting. All of this characteristics are more similar to Eu–enrichment type anatetic charnockites, but the mafic granulite delamination occurring in lower crustal that the partial melting happened can formation the evolution of Eu–depletion anomaly characteristic (Gao et al., 1997; Gao et al.,1999). It is inconsistent with the Eu anomaly characteristic indicated that the source of anatetic charnockite is not only the mafic material in this paper. The digrama of SiO2 vs. A/CNK consistent with the composition of the water–bearing melt at high temperature (Fig.11a, Sisson et al., 2005), indicating the charnockites in this study area may be have a water–bearing basaltic source rock, and having the mixed composition characteristics of the experiment sample of Beard and Lofgren.(1991), Rapp and Watson. (1995) and Sisson et al.(2005).

Experimental petrology studies indicated that granitic magma can be formed from a large number of common rocks under widely temperature and pressure conditions, in view of the different geochemical identification markers to discriminate the different components of protoliths (Rajesh and Santosh., 2004). The compositional difference of partial melts pro–from sources, such as greywackes, pelites, and amphibolites can be visualized (Fig.15). It follows from figure 15 that the original melt of the NCC charnokitesss may be derived from an mafic pellite and amphibolitic source. Experimental studies raise to the partial melting of hydrous basalt can produce the low Mg# magmas (Mg#<45), regardless of the pressure conditions (Rapp et al.,1991; Rapp and Watson 1995), further supporting the Ferroan– charnockite original of crystal fractionation of associated shoshonitic magma that the more basaltic sources than mafic, and all of them has a amphibolite volcanic original rocks (Fig.15). In anatetic charnockite, Eu–enrichment type samples of has the characteristics of high–Mg content (#Mg>45) that revealing the more mafic pellites sources than basalt (Rapp et al,. 1991; Rapp and Watson 1995). However, Eu– depletion type has characteristics of amphibolite volcanic original rocks, and more likely a basaltic source and mantle material addition.

Figure.15 The diagram of the Al2O3/(FeO+MgO+TiO2) wt.% vs. Al2O3+FeO+MgO+TiO2 (wt.%) in Eu enrichment

type and Eu depletion type charnockite samples from the north margin from NCC Rejesh and Santosh. (2004).


Table 1 Geochemical characteristics of charnockite in the northern margin of NCC

Geochemical Numbers Eu/Eu* SiO2

(wt.%)

CaO

(wt.%)

CaO+Na2O

(wt.%)

FeOT

(wt.%) K2O

(wt.%) K2O/Na2O

K2O+Na2O

(wt.%)

TiO2

(wt.%)

Nb

(ppm) ∑REE(ppm) (La/Yb)N Mg# HFSE LILE

SHY

Charnockite

Eu

enrichment 5 1.07~3.18 70.3~73.9 1.64~2.61 4.28~5.61 1.62~3.26 2.80~5.36 0.93~2.00 5.80~8.64 0.25~0.48 2.0~30.0 54.2~160.0 17.5~77.4 34.6~ 40.0 Low Th

Low Sr

High K

Eu depletion 4 0.35~0.95 64.4~73.3 3.48~5.11 3.49~4.72 1.91~5.25 3.61~6.57 1.02~2.42 6.50~9.50 0.15~0.57 2.0~18.0 149.1~370.8 10.8~92.9 7.33~48.7 High Th High Sr

Low K

BQG

Charnockite Eu depletion 8 0.45~0.99 57.4~72.2 1.30~4.77 4.34~9.14 2.80~7.40 2.50~5.77 0.66~1.98 6.39~8.11 0.30~1.10 0.7~16.0 104.9~481.3 13.5~50.4 36.3~48.9 – –

XWLBL

Charnockite

Eu

enrichment 8 1.24~3.62 65.4~71.4 4.00~5.43 4.43~6.45 1.67~3.54 0.41~1.13 0.09~0.26 4.67~6.04 0.04~0.48 0.9~4.1 40.68~56.23 13.5~45.0 44.0~54.0 Low U, Th

Low K

High Sr

Eu depletion 8 0.60~0.96 59.4~64.8 5.07~6.76 7.62~9.33 4.38~8.14 0.52~1.63 0.16~0.53 3.98~6.13 0.43~0.67 4.4~8.0 75.2~220.3 15.7~74.8 45.0~57.0 High U,Th High K

Low Sr

LYS

Charnockite

Eu

enrichment 6 1.28~4.39 62.3~72.8 3.48~5.11 7.62~9.33 0.85~3.73 3.61~6.59 1.02~2.44 6.50~9.52 0.06~0.59 5.0~9.5 112.2 ~160.5 14.8~27.2 41.9~71.9 Low U,Th

High K

Low Sr

Eu depletion 6 0.67~0.94 59.6~62.4 5.28~5.89 9.24~10.39 2.12~3.2 2.80~5.39 0.93~2.03 5.80~8.67 0.23~1.15 5.9~15.0 112.2 ~160.6 12.9~19.5 40.0~57.9 High U,Th Low K

High Sr

CKS

Charnockite

Eu

enrichment 10 1.24~4.41 57.5~71.7 3.06~5.07 6.44~9.45 1.74~7.52 3.68~6.58 1.01~1.99 6.44~9.45 0.22~0.86 3.3~9.3 56.8~112.7 13.5~45.0 44.0~59.0 High Th

High K

Low Sr

Eu depletion 5 0.92~1.0 62.3~70.3 3.5~13.7 5.06~7.09 3.52~10.6 0.84~2.59 0.19~0.58 5.06~7.09 0.28~1.26 3.8~7.6 107.6~168.2 4.0~12.6 45.0~62.0 Low Th Low K

High Sr

JN

Charnockite

Eu

enrichment 5 1.07~1.90 62.5~71.8 1.25~3.78 4.43~6.45 1.69~3.11 3.68~6.58 1.01~1.93 7.34~9.99 0.30~1.39 2.2~17.0 135.5~372.5 19.1~54.2 14.0~43.0 High U,Th

High K

Low Sr

Eu depletion 5 0.49~0.94 54.9~67.3 3.11~6.73 7.31~11.41 4.83~9.26 1.20~3.60 0.26~1.20 5.61~7.25 0.74~1.69 15.0~20.0 236.4~389.5 6.2~18.1 37.0~47.0 Low U, Th Low K

High Sr

GHY

Tonalite

Eu

enrichment 9 1.07~1.90 68.5~72.5 2.29~5.07 6.81~8.71 1.21~2.21 3.61~6.62 0.22~0.62 4.98~7.31 0.12~0.39 1.7~3.3 31.6~149 32.3~52.5 25.8~68.3 – –

GHY

Charnockite

Eu

enrichment 15 0.90~1.02 57.5~66.5 2.94~5.41 7.96~10.54 3.97~6.23 1.09~3.08 0.25~0.68 4.12~7.98 0.30~0.70 4.9~11.0 35.6~146.4 7.3~19.4 41.0~54.0 High Th

Low K

High Sr

Eu depletion 11 1.0~4.34 55.0~68.3 0.66~9.15 4.83~10.18 4.21~9.27 0.87~3.27 0.19~0.78 4.25~6.65 0.20~0.92 2.4~9.5 126.7~246.0 6.5~52.5 43.0~72.0 Low Th High K

Low Sr


The chemical compositions of charnockite samples from NCC seem to have an extensive compatibility with mafic pellites and basaltic source, especially the anatetic charnockite. Frost and Frost. (2008) studies considered that comparing with the basalt, ferrodiorit is more likely to be the protolith of charnockites formed by crustal melting, because of its melting point is lower than basalt, and iron ferro–basalts more exists in extensional environments. Experimental petrological study shows that mainly composition of ferrodioritic source compositions melts is monzonite (Scoates et al., 1996), while the opx–bearing monzonites have not been found among the NCC charnockites considered in this study (Le Maitre., 2002). The coexistence of Eu–enrichment and Eu–depletion geochemical characteristics are more similar to South India intermediate–felsic charnockite (Chacko et al., 1992; Rajesh, 2012). Therefore, we considered that the anatetic charnockite may be has a part of basaltic sources. Eu anomaly of anatetic charnockite is especially prominent and becomes a typical character of most of the anatetic rocks. In addition to the mineralogical explanation above, we are trying to make a further studiy from the sources. Strongly peraluminous melts (A/CNK > 1.1), like Southern India Nilgiri garnetiferous charnockites, all of them are commonly taken to have formed by a sedimentary sources (Chappell and White.,1974). However, the anatetic charnokites in this paper has a metaluminous to week peraluminous characteristics (A/CNK < 1.1), and the use of a different set of geochemical discrimination factors does not rule out the igneous affinity of the source rock of NCC charnokites (Fig.16). Further more, igneous enclaves present within both Eu–enrichment and Eu–depletion type anatetic charnokites from the NCC indicates that more mafic magmas and/or other igneous sources may have been involved in the origin of both types of magma.

Figure. 16 Plots illustrating the igneous affinity of Eu–depletion and Eu–enrichment type charnockites from NCC.

The igneous–sedimentary dividing lines in the TiO2 vs.SiO2 plot and Na2O/Al2O3 vs. K2O/Al2O3 plot are from

Tarney. (1976) and Barrels and MacKenzie. (1971). The legend is the same as Figure 11.

Previously geochemical views indicated that metafily wackes, felix orthogneises and amphibolites possible become source for the production of the peraluminous charnockites. There are also tending to produce only small quantities of strongly peraluminous melting (A/CNK >1.3) shown by Pelitic sediments melting experiments, however, they are not suggesting as the mainly source for the NCC anatetic charnockites melts with lower A/CNK values (usually < 1.1). Futher more, previous study shown that the K2O/Na2O ratio of a pelitic source melting is much higher (Montel and Vielzeuf., 1997, average of K2O/Na2O ratio: 4–24) than the ratio in the least evolved samples of NCC Eu riched and Eu depleted type anatetic charnockite which the Eu–enrichment type (K2O/Na2O: 0.94–1.03) higher than Eu–depletion type (K2O/Na2O: 0.83–0.97) in Table 1. We can see the Eu–enrichment type anatetic charnockites have more mafic pelites sources, however, Eu–depletion type has the more sources of amphibolitic rocks sources in Figure 15. The more feldspar and quartz riched metagreywackes and orthogneisses are potentially fertile sources and could be produced a relatively large volumes of moderately peraluminous melts (Fig.15), the production of differences composition of partial melts derived from greywackes, pelites and amphibolites can be found visualized. And we can see in the Figure 15, the original melting of the anatetic charnockites may be derived from an amphibolitic rocks and mafic pelites sources, and the Eu anomaly characteristic may be related to the content of amphibolitic rocks and mafic pelites, also influenced by the underplating of Sr and Ba–riched mafic magma. The similar affinity of the parent rocks for the anatetic charnockites from the NCC and the India South high Ba–Sr charnockites massifs (Rajesh, 2004) are substantiated by their similarity to high Ba–Sr granitoids with low K2O/Na2O ratios (Fig. 12b) and other elemental characteristics (Supplementary Table1, high content of Sr, Ba and LREE, the low Y and HREE, elevated La/Yb) that are typical of adakites and Archaean TTG suites (Fig.12b, Martin.,1986; Drummond and Defant.,1990). This character is different from those of charnockites fractional crystallization product of shoshonitic magma, like those of the SHY and JN Eu–depleted massif, which show a similarity to high Ba–Sr granitoids with low Ba and high Y ratios (Fig.10, 12).


The feature of Nb depletion has considered to be a typical crustal sources rock. All of the geochemical discussion above, considered that Eu–enrichment samples have a mafic pellites sources and Eu–depletion samples have a protolith of basaltic rock for anatetic charnockites. With a widely variety of pressures, the experiments of amphibolite dehydration melting generate a TTGs magmas conducted at 750–1000℃ (Rushmer.,1991; Beard and Lofgren., 1991; Patiño Douce and Beard.,1995), which has a similar or indistinguishable compositions of charnockites studied in this study. The degree of partial melting and residual mineral assemblages are controlled by the heat ultimately (Rajesh et al., 2004). Dehydration melting experiments showed that hornblende is absolutely consumed at the temperature of 925–1000℃, leaving a granulitic residue mineral association of orthopyroxene, clinopyroxene, plagioclase and Fe–Ti oxides with garnet at higher pressures (Rushmer.,1991). When the temperatures of the melting is higher, the remaining minerals partially consumed (Rajesh et al., 2004). Although the latter stage of partial melting is mainly the plagioclase, and residual mineral assemblage remains is not changed under a condition of the isobaric temperature increase. Most experiment of metabasaltic sources dehydration melts are strongly peraluminous (Patiño Douce.,1997), however, dehydration melts will be produced from metabasaltic sources at a very high temperature of partial melting (>1000℃), the melting start to have a metaluminous characteristic (Rapp et al.,1991). The characteristic of low contents of K2O, a relatively high contents of Na2O and the values of Mg#, whatever the degree of partial melting, making the meta–basaltic rock suitable source rocks for anatetic charnockites.

Figure.17 AFM (wt.%) plot of the NCC anatetic charnockites and experimental data on compositions of partial

melts derived from a variety of crustal and mantle rocks by water–under saturated melting. The different rocks are

from: Dacite (Conrad et al., 1988); Basalt (Beard and Lofgren.,1991); Basaltic andesite (Beard and Lofgren.,1991);

Tonalitic gneiss (Skjerlie et al.,1993); Metapelite (Skjerlie et al., 1993); Tonalitic gneiss (F–rich) (Skjerlie et al.,

1993); Charnockite (Beard et al., 1994); Charnockite (CO2–rich) (Beard et al., 1994); Quartz amphibolite (Patiño

Douce and Beard., 1995); Tonalite (Patiño Douce., 1997); Granodiorite (Patiño Douce., 1997); #Charnockite

(Litvinovsky et al., 2000); Alkali basalt (Kaszuba and Wendlandt., 2000). The respective compositions of the

starting material (indicated by arrow) and the product(s) of water–under saturated melting of some of these rocks

are shown (by similar symbols).

Experiments of dehydration melting by using the basaltic starting materials yielded melts is similar to the NCC (Fig.17, Beard and Lofgren’s., 1991), and the experiments of Springer and Seck (1997) studies also using basaltic starting material showed that with rising temperatures at constant CO2 content, and it is also similar to the southern India intermediate charnockites. The experiments of Kaszuba and Wendlandt (2000) indicated that with increaseing the content of CO2 at the constant–temperature, similar to the most evolvement of anatetic charnockites that the melts become richer in the content of normative orthoclase. Besides, the CO2 riched melt is more likely to enrich in K, Ba, and Zr (Eggler et al., 1987) that CO2 riched fluid inclusions have referred from some charnockite (Touret and Hansteen 1988; Srikantappa., 1996; Santosh et al., 2003; Rajesh., 2004), and it is similar to the characteristic of anatetic charnockites from North China (Fig.8). Same as the southern India charnockites, lacking of K–depletion and extreme Rb–depletion in some of the high tempreture–pressure Archaean charnockites from NCC may also mirror a fluid phase existence with a relatively higher ratios of the CO2/H2O (Weaver et al., 1980; Condie and Allen.,1984).

In the case of Eu–depletion type and Eu–enrichment type anatetic charnockites massifs and granulite showing close spatial association (and possibly temporal) from NCC, the characteristics of their near continuous variations in geochemistry compositions probably point out a genetic relationship between them (Shi et al., 2018; Shi et al., 2019a). If these two types of charnockites were distinguished from the similar parent magmas, the Eu–depletion charnockites may presumably represent a higher degree of separation and crystallization. For Eu–depletion charnockites, the absence or lower Eu anomalies may not develope a large number of fractionation requirement for most of the charnockite formation (Rajesh., 2004). The constant ratios of the trace elements (Ce/Zr, Zr/Nb and Rb/Zr) is often considered to be the dominant process in the evolution of specific suites (Wilson., 1989). Obviously the crustal


melting and contamination are unlikely occurred, in the event of the ratio of trace elements remains in a suite. For the NCC charnockites, the above mentioned characteristics of trace element ratios vary in both Eu–depletion and Eu–enrichment type charnockites. The separation and crystallization model can be argued against by some bimodality of the charnockite (eg. Pallavaram massif, with basic membere). So, the separation and crystallization might not be responsible for contrasts among Eu–depletion and Eu–enrichment type anatetic charnockites of the same rocks. For example, this would explain the Eu–depletion and Eu–enrichment characteristics and raise in the abundances of REE that correlate with the increasing of the content of the SiO2 in some charnockites. Such comparison may influenced by the distrinct degree of melting with lower degree melting point having a higher contents of the SiO2 and HREE, and also characterized by the upwarping of the tail of the distribution curve of HREE. It is possible to explain the spatial association of Eu–enrichment and Eu–depletion anatetic type charnockites by a two–stage model, assuming an original lower degree of the partial melting and subsequent crystallization fractionation. We can not get rid of the origin of fractional rather than batch melting for the formation of those charnockites, having the REE patterns with a characteristics of slightly positive Eu anomaly. The model indicated that the different melting ratio of the mafic pellites and basalts in the anatetic charnockites that the formation of mineral composition and content are different, and forming the unique Eu anomaly characteristics in the anatetic charnockites. 6.2 Tectonic significance

Geochemical characteristics and the core–mantle–rim structure of zircon in charnockites further constrain metamorphic anatexis. Extensive U–Pb zircon geochronology studies have assessed the morphology, internal structure, and Th/U ratio of zircon in various rocks (Rubatto et al., 1999; Rubatto, 2002; Hoskin and Schaltegger, 2003; Geisler et al., 2007; Wan et al., 2011; Zhao et al., 2015). Previously study obtained abundant achievements in the chronology of charnockites in the northern margin of the NCC. JN Charnockite and retrograded biotite–hornblende gneiss obtained anatetic ages of 2469±9Ma~2492±29Ma (Shi et al., 2019c), occuring in the stage of prograde granulite facies metamorphism, in which the formation of charnockite is closely related to ~2.5Ga granulite facies metamorphism in the northern margin of NCC. Ma et al. (2013a) and Zhang et al. (2014) study shown that the XWLBL charnockite is the anatetic product of basic granulite, and obtained crystallization age of remelted magma at 2511±12Ma~2512±10Ma and 2490±14Ma~2490±5Ma. LYS Charnockite obtained an anatetic ages of 2478±12Ma~2498±22Ma, indicating a stage of prograde ~2.5Ga isothermal decompression after peak metamorphism granulite facies (Dong et al., 2012a; Liu et al., 2017; Shi et al., 2019a). Xu et al.(2013) study for SHY Eu–depletion type Magnesian–charnockite obtained diagenetic ages of 2484±7Ma~2494±12Ma, Liu et al.(2017) obtained magmatic crystallization age of 2455±15Ma from SHY Eu–enrichment type Ferroan–charnockite. GHY Charnockite obtained a magmatic crystallization zircon age of 2502±10Ma~2512±12Ma and a metamaphism zircon ages of 2484±36Ma in GHY Hy–Tonalites (Zhang et al., 2017). Previously study indicated that Yinshan Block was affected by magmatism event at ~2.5Ga (Tabel 2), and the Archean U–Pb zircon ages obtained from a wide range of high–grade metamaphism rocks. Guyang complex composed of the Meta–dacites (2516~2500Ma, Chen, 2007), diorites and granitoids (2556~2520Ma, Jian et al., 2012) and sanukitoid high–grade metamorphism rock (2523~2465Ma, Ma et al., 2013b); Meta–gabbro and charnockites suites of XWLBL Complex obtained the ages of 2540~2500Ma (Zhang et al., 2014); Orthopyroxene–bearing TTG gneisses also obtained the ages of 2545~2507 Ma in Wuchuan Complex (Dong et al., 2012b); Meta–sandstones obtained the ages of 2690–2450Ma from the Huade Group (Liu et al., 2012); Orthogneisses from the Hongqiyingzi Group obtained the ages of 2535~2484 Ma and Sandstones from the Zhaertai Group obtained the ages of ~2500Ma (Li et al., 2007). A set of common Komatite–Greenschist–TTG–Metamorphic gabbro–charnockite in the process of subduction–collision–extension evolution has been identified in the northern Guyang–Xiashihao– Wuchuan (Ma et al., 2013a; Ma et al., 2013b; Ma et al., 2016), and it is generally believed that the subduction and collision tectonic evolution of the oceanic crust took place from north to south in Wuchuan–Xiwulanbulang–Guyang area. The Archean basement of Shiguai (Wan et al., 2009, 2013a, 2013b, 2015; Cai et al., 2014; Xu et al., 2015)–Daqingshan (Wan et al., 2013a; Xu et al., 2015; Ma et al., 2015; Liu et al., 2012; Liu et al., 2017)–Wulashan (Cai et al., 2014)–Jining (Shi et al., 2018, 2019a)–Siziwangqi (Chen et al., 2017)–Gehuyao (Zhang et al., 2017) obtained isotope chronology metamaphic ages of ~2.5Ga and ~2.45Ga (Fig18). The ocean crust subduction collision orogenic event occurred in Yinshan block to ~2.5Ga in NCC (Bai et al., 2015; Yang et al., 2016), and detail of subduction–collision–extension of the current orogenic event (Ma et al., 2013a; Ma et al., 2013b; Ma et al., 2013c; Ma et al., 2016). Island arc environment after subduction of oceanic crust at 2.52~2.49Ga, with a large number of TTG and diorites, accompanied by a large number of charnockites associated with island arcs. During the 2.47~2.44 Ga, the ocean crustal closure and collisional orogeny development, with the mantle–derived magma underplating in extensional environment (Xu et al., 2013; Ma et al., 2013c; Nancy Chen et al., 2017; Zhang et al., 2017; Shi et al., 2018; Shi et al., 2019a).


Table 2 zircon U–Pb age and Hf–Nd isotope statistics in North China Craton

Rock Location Age

(Ma)

Metamorphic

Age(Ma) εHf

TDM

(Ma) Method Data from

Metamorphic

Complex

XWLBL

Charnockite

E 110°42′00″

N 40°57′00″ 2533±15 2490 ±11 +2.3 ~ +5.5 2648~2779 LA–ICP–MS Ma et al., 2013b

E 110°42′00″

N 40°57′00″ 2524±17 2498 ± 3 +1.4 ~ +4.9 2631~2749 LA–ICP–MS Ma et al., 2013b

E 110°55′12″

N 41°07′31″ 2512 ± 10 –1.4 ~ +2.3 2712~2782 LA–ICP–MS Zhang et al., 2014

E110°54′06′

N 41°03′12′′ 2525 ± 8 SHRIMP Jian et al., 2012

LYS Charnockite

E 110°55'25″

N 41°04'19″ 2548±24 2496 ± 36 –4.21 ~ +7.36 2649~2806 SHRIMP Ma et al., 2013

E 110°45'43″

N 40°55'47″

2506 ± 9

2479 ± 12 ~1.6~+8.09 2645~2880 SHRIMP

Dong et al., 2012b;

Ma et al., 2013c

JN Charnockite

E 118°56′49"

N 41°01′08" 2469 ± 9 SHRIMP Shi et al., 2019

E118°57′18"

N 41°00′55" 2474 ± 15 SHRIMP Shi et al., 2019

E112°35′26"

N41°04′02" 2492 ± 29 SHRIMP Shi et al., 2019

SHY Charnockite

E110°54′06′

N 41°03′12′′ 2484 ± 7

2494 ±12 +0.22 ~ +3.92 2608~2782 SHRIMP Xu et al., 2015

E110°18′06′

N 40°43′12′′ 2455 ± 8 –9.74 ~ +3.56 2522~2642 SHRIMP Liu et al., 2017

BQG Charnockite E110°18′06′

N 40°43′12′′ 2455±15 Ma +0.22 ~ +3.92 2602~2674 SHRIMP Liu et al., 2017

CKS Charnockite

E109°41′52′

N 40°41′56′′ 2484± 6 +3.7 ~ +7.0 2532~2658 SHRIMP Ma et al., 2012

E109°33′52′

N 40°56′56′′ 2484±6

Single

Zircon Wang et al., 2001

GHY Charnockite E114°25′06′′

N 40°15′12′′ 2502 ± 10

2512 ± 12 LA–ICP–MS Zhang et al., 2017

GHY Hypersthene

Tonalite

E114°25′16′′

N 40°17′23′′ 2502 ± 10

2512 ± 12 LA–ICP–MS Zhang et al., 2017

Gneiss

E110°28′13′

N 40°39′16′′ 2459 ± 7

2454 ± 7 3.39 ~ +6.29 2564~2624 LA–ICP–MS Liu et al., 2017

E109°30′34′

N 40°41′27′′ 2432 ± 29 –0.2 ~ +8.4 2015~2606 SHRIMP Ma et al., 2012

E109°38′29″

N 40°42′40″ 2444 ± 9 –4.9 ~ +7.4 2478~2656 SHRIMP Ma et al., 2012

Granulite

E109°40′37″

N 41°34′40″ 2452 ± 8 SHRIMP Cai et al., 2012

E 110°45'43″

N 40°55'47″ 2545 ±10 2503 ±10 –2.30 ~ +6.49 2634~2757 SHRIMP

Dong et al., 2012a;

Ma et al., 2013c

E 110°34'12″

N 41°10'07″ 2511 ± 5 Camara Zhang et al., 2005

E 110°35'05″

N 40°57'59″ 2512 ±16 LA–ICP–MS Liu et al., 2016

E 110°35'05″

N 40°57'59″ 2517 ± 6 LA–ICP–MS Liu et al., 2016

E 110°51'03″

N 41°05'24″ 2544 ± 5 2503 ±12 SHRIMP Jian et al., 2012

Granitoid

Diorite E 110°39'41″

N 41°17'23″ 2503 ± 7 –0.66 ~ +4.44 SHRIMP Ma et al., 2013

sanukitoid E 110°45'43″

N 40°57'28″ 2523 ± 7 1.5 ~ +6.3 LA–ICP–MS Ma et al., 2013b

sanukitoid E 110°09'48″

N 41°06'05″ 2520 ± 9 SHRIMP Jian et al., 2012

TTG E 110°06'14″

N 41°31'34″ 2534 ± 7 SHRIMP Ren et al.,2010

TTG E 110°00'18″

N 41°18'20″ 2515 ± 6 SHRIMP Jian et al, 2012

Greenstone Belt

Trondhjemite E 110°55' 23″

N 41°07' 50″ 2528 ± 16 1.06 ~ +8.83 SHRIMP Jian et al,2012b

Andesite E 110°35' 50″

N 41°02' 02″ 2510 ± 7 SHRIMP Jian et al, 2012b

Basalt E 110°34' 09″

N 41°02' 02″ 2516 ± 10 LA–ICP–MS Chen et al., 2007

High–Mg Andesit E 110°35' 50″

N 41°02' 02 2533 ± 5 SHRIMP Jian et al., 2012

Adakite E 110°32' 13″

N 40°57' 57″ 2556 ± 6 SHRIMP Jian et al, 2012

Basalt E 110°33' 58″

N 41°08' 59″ 2562 ± 14 Camerca Liu et al., 2012


Rajesh and Santosh (2004) and Rajesh (2012) studies have shown that anatexis can occur in various tectonic settings, mainly in continental arcs and collision zones. It is a reflection of the change of temperature and pressure conditions, with a concomitant phenomenon of high–grade metamorphism. These studies suggest that charnockite is a key to understand the lower crustal processes, discussing the petrogenesis and tectonic environment during its formation, geological significance to elucidate the growth and tectonic evolution of the early crust (Janardhan et al., 1982; Santosh and Yoshida, 1992; Frost et al., 2000; Kar et al., 2003; Rajesh, 2012; Rajesh and Santosh, 2012; Yang et al., 2014; Zhang et al., 2014). Geochemical studies suggest that the Ferroan–charnockite may be formed in extensional tectonic environment and the Magnesian–charnockite may be formed in magmatic arc environment (Frost and Frost 2008; Rajesh and Santosh, 2012; Rajesh, 2012). Peng et al. (2012) raised to a dominant origin from in situ melting of metamorphic sediments for the paleoproterozoic charnockites from the NCC, in which can not suit to these situation. Lacking of the obviously sedimentary sequences in the Yinshan Block of NCC during the Neoarchean, and the geochemistry elemental inconsistency inconsiste with the production of the sediment melts and the metaluminous characteristics of the anatetic charnockites (Table 1), with the contrast of evolved isotopic geochemistry compositions between the juvenile crustal formation charnockites and meta–volcanic rocks (Table 2). JN Eu–depletion type and SHY Eu–depletion type Charnockite has the characteristics of Ferroan–charnockite (Fig.6), while the anatetic charnockites has the feature of Magnesian– charnockite (Fig.6). Frost (2008) study summarized the genetic background model for Indian charnockite, for fearron charnokitess, the heat and fluids released from mafic magma that has ponded at the base of the crust have produced granulite metamorphism in the lower crust under an extensional tecnotic environment. However, there are also an characteristic of arc environments for magnesian charnokitess which melting of the juvenile lower crust by the mantle magma underplating. Rajesh (2012) raised the South India charnockites related to the mantle basaltic magma underplating, with the converge of alkaline characteristics mafic magmas, and the charnockite formed be the partial melting of mafic lower crust. Upwelling of the basaltic magma with low water content might occur to dehydration melting of the lower crust formation the charnockite. In summary, combining with the understanding of the genetic model of Magnesian–Ferroan–charnockite in southern India (Frost et al., 2001) and the results on previous isotopic geochronology and geochemistry research, we consider that Late Neoarchean charnockites in the northern margin of the NCC, mainly related to the regional tectonic events of ~2.5Ga and ~2.45Ga (Fig18).

Figure.18 Charnockites from Northern margin of NCC in terms of Age histogram diagram (Data from: Li et al,

2011; Guo et al, 2012; Jian et al., 2012; Xu et al., 2013; Ma et al., 2013a; Ma et al., 2013b; Ma et al., 2013c; Liu

et al., 2013; Cai et al., 2014; Zhang et al., 2014; Bai et al., 2015; Xu et al., 2015; Ma et al., 2016; Yang et al.,

2016; Geng et al., 2016; Chen et al., 2017; Zhang et al., 2017; Liu et al., 2017; Shi et al., 2018; Shi et al., 2019c)

In this paper, the formation of anatetic (Magnesian) charnockite is more likely related to the generally ~2.5Ga subduction of the oceanic crust in the northern margin of the NCC. Comparing with the geochemistry and isotope chronology achievements, and the mantle–derived magma associated with the arc may have formed in the island–arc environment after the subduction of the oceanic crust, with the anatexis of the younger basaltic lower crustal and the mafic pellites magma by the upwelling of anatetic melts. The anatetic charnockites are closely associated with the intermediate–basic granulite in space and transitional gradually (Fig. 19a), forming of the difference of composition of melting, with the coexistence of Eu–enrichment and Eu–depletion type of REE characteristics (Fig. 19a). The formation of Ferroan–charnockite (SHY Eu–depletion and JN Eu–depletion type Charnockites) might be related to the ~2.45Ga tectonic event of NCC. We refer to the crustal thinning and pressure reduction inluenced by the underplating of basaltic shoshonitic magma and the crystallization


differentiation of the melting under the back–arc extension environment of collision orogeny, and the addition of crustal source materials plays an important role (Fig. 19b).

Figure.19 Proposed tectonic model showing the late Neoarchean subduction–related arc magmatismin from

Northern margin of NCC. (a) Maturation of the arc system and emplacement of voluminous Greenstones, TTG and

Anatetic Charnockites( ~2.5 Ga); (b) The accretion of the arc system to the northern margin of the NCC possibly

back–arc basin formation. Upwelling of hot asthenospheric mantle induced the products of Charnockites(~2.45Ga)

by crystal fractionation of associated shoshonitic magma derived from melting of an lithospheric mantle(Modified

after Chen et al., 2017).

7 Conclusions

(1) The distribution of major and trace elements in charnockite is very uneven. Significant depletion in LILEs (eg. Cs, U, Th), enrichment in Sr, depletion in HFSEs (eg. Nb, Ta, P, Ti). With the coexistence of Eu enrichment and Eu depletion type of REE patterns. Eu–enrichment type samples is relatively high content of plagioclase and low content of the dark mineral. The relative decrease of total REE may be affected by the remnants minerals of refractory by zircon and apatite.

(2) The anatexis of the younger basaltic lower crustal sources and mafic pellites sources, formation the characteristics of anatetic Magnesian–charnockite in NCC, with the upwelling of mantle magma. The difference ratios of mafic pellites and basalts sources involved in anatetic melting, resulting in the coexistence characteristics of Eu enrichment and Eu depletion REE patterns. Ferroan–charnockite is the product of the upwelling of mantle–derived shoshonitic magma and the crystallization differentiation of the melting.

(3) Anatetic Magnesian–charnockite might be related to the magmatic island arc environment after subduction of the NCC ~2.5Ga oceanic crust event, and the anatetic occurred at the post–peak stage of granulite metamorphism. Ferroan–charnockite may be formed by crystallization differentiation of the shoshonitic magma under the ~2.45Ga back–arc extension environment of collision orogeny.

Acknowledgements The authors acknowledge the anonymous referees for their constructive suggestions and comments,

which helped to improve the paper

Funding This work was financially supported by the National Natural Science Foundation of China

(41872194, 41872203).


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About the first author SHI Qiang, male, born in 1992 in Anshan City, Liaoning Province;doctoral candidate; study in Jilin university;

research assistant of structural geology, College of Earth Sciences. He is now interested in the study on Early

precambrian metamorphic tectonic evolution, and garnet-bearing granite. Email: [email protected]; phone:

13578720423.

About the corresponding author XU Zhongyuan, male, born in 1958 in Datong City, Shanxi Province; master; graduated from Jilin university;

research assistant ofstructural geology, College of Earth Sciences. He is now interested in the study on Early

precambrian metamorphic tectonic evolution of North China Craton. E-mail: [email protected]; phone:

13844161972.


Supplementary Table 1 The relevant parameters of major elements (wt.%) and trace elements (ppm) in

charnockites of NCC

Sample SHY–

1 SHY–2 SHY–3 SHY–4 SHY–5 SHY–6 SHY-

7

SHY–

8

SHY–

9

BQG–

1

BQG

–2

BQG–

3

BQG–

4

Rock SHY Charnockite BQG Charnockite

SiO2 73.28 72.74 66.39 71.70 71.43 64.86 70.96 72.39 73.89 61.89 62.93 64.74 66.62

TiO2 0.38 0.10 0.57 0.27 0.21 0.44 0.39 0.30 0.05 1.10 0.59 0.66 0.57

Al2O3 12.31 13.52 15.37 14.13 14.27 15.08 14.22 14.21 13.35 15.45 15.33 15.63 15.20

FeOT 3.99 4.95 5.25 1.91 1.67 3.52 2.69 2.02 1.76 6.18 5.28 4.52 3.99

MnO 0.03 0.03 0.06 0.02 0.02 0.04 0.02 0.02 0.03 0.10 0.10 0.08 0.05

MgO 0.31 0.22 2.80 0.70 0.52 1.87 0.47 0.60 0.99 1.98 2.94 1.52 1.25

CaO 1.23 0.92 1.19 1.78 1.85 3.62 1.48 1.68 2.61 2.85 3.74 3.67 2.80

Na2O 3.00 3.50 3.53 3.22 3.28 3.48 3.28 2.60 3.00 3.04 4.31 3.77 3.60

K2O 4.80 6.00 3.61 5.23 5.36 4.67 5.98 5.20 2.80 5.77 3.35 3.48 3.83

P2O5 0.05 0.05 0.07 0.11 0.06 0.30 0.09 0.20 0.20 0.46 0.20 0.28 0.22

LIO 1.56 0.22 1.40 0.88 1.13 1.27 0.81 0.90 1.95 0.70 0.77 1.11 1.33

Total 101.22 102.53 100.61 100.03 99.88 99.33 100.56 100.21 100.72 99.69 99.74 99.67 99.65

Na2O+K2O 7.80 9.50 7.14 8.45 8.64 8.15 9.26 7.80 5.80 8.81 7.66 7.25 7.43

K2O/Na2O 1.60 1.71 1.02 1.62 1.63 1.34 1.82 2.00 0.93 1.90 0.78 0.92 1.06

Mg# 12.20 7.33 48.70 39.50 35.70 48.60 23.80 34.60 50.10 36.30 49.80 37.50 35.80

A/CNK 0.99 0.97 1.29 0.99 0.98 0.87 0.98 1.09 1.05 0.94 0.87 0.94 1.00

Ba 470.1 442.3 887.6 786.4 746.8 721.2 1816.0 1231.0 759.8 1576.0 1052.

0

1502.

0 1792.0

Cr 200.7 18.3 144.9 25.5 10.5 48.8 142.9 12.4 37.2 5.0 59.6 18.8 21.5

Sr 531.2 154.2 437.0 389.0 348.0 414.0 601.0 438.5 397.2 307.0 421.0 459.0 504.0

V 65.5 27.9 90.1 24.5 7.9 40.7 81.4 12.6 39.0 51.8 104.0 69.2 51.5

Zr 97.2 183.9 125.0 77.0 3.0 148.0 315.4 161.1 129.2 736.0 176.0 337.0 204.0

Rb 18.9 49.0 84.0 185.0 219.0 141.0 88.5 124.0 26.9 152.8 109.3 65.7 78.1

U – – – – – – – – – – – – –

Th 15.39 7.72 6.00 5.00 18.00 14.00 14.91 2.48 6.81 13.00 5.00 2.20 <1

Ta 3.45 2.12 <5 <5 <5 <5 2.38 0.86 1.27 16.10 4.80 0.62 0.62

Hf – – – – – – – – – 27.90 12.60 7.90 5.00

Nb 17.97 15.34 5.00 <2 <2 <2 16.54 5.42 17.50 1.70 0.70 15.70 12.10

La 82.93 72.81 33.56 17.53 13.87 49.30 53.67 40.85 24.46 105.40 37.84 67.29 37.20

Ce 160.80 139.70 63.44 29.40 22.91 92.90 102.75 73.48 38.62 215.00 73.96 149.6

0 74.08

Pr 22.13 19.71 7.30 2.08 2.35 11.35 10.83 8.27 5.09 24.73 8.42 18.95 9.00

Nd 74.62 63.42 27.99 10.48 9.06 42.63 37.70 27.10 14.75 87.22 27.25 69.12 33.24

Sm 12.15 10.64 4.99 1.67 1.73 6.63 4.83 3.79 2.07 14.85 4.77 11.94 5.71

Eu 1.16 1.08 1.13 0.87 0.95 1.08 1.14 1.10 1.20 2.92 1.10 2.18 1.73

Gd 8.44 7.57 4.40 1.15 1.18 4.51 2.81 2.64 1.38 10.69 3.67 8.61 4.48

Tb 0.98 0.86 0.55 0.30 0.30 0.41 0.30 0.31 0.17 1.59 0.57 1.38 0.65

Dy 4.46 3.04 3.25 0.61 0.68 2.38 1.24 1.25 0.60 8.14 3.05 6.96 2.97

Ho 0.66 0.55 0.70 0.12 0.14 0.49 0.28 0.23 0.12 1.52 0.60 1.27 0.56

Er 1.35 1.07 1.88 0.26 0.39 1.21 0.64 0.57 0.32 4.24 1.75 3.59 1.40

Tm 0.18 0.13 0.27 0.10 0.10 0.15 0.10 0.06 0.04 0.63 0.27 0.50 0.19

Yb 0.79 0.50 1.88 0.26 0.48 0.95 0.45 0.32 0.23 3.82 1.68 3.03 1.05

Lu 0.11 0.07 0.30 0.10 0.10 0.16 0.10 0.06 0.04 0.56 0.25 0.41 0.15

Y 12.18 9.66 18.32 3.15 3.80 11.47 4.77 5.06 2.88 38.36 16.15 35.64 14.04

∑REE 370.76 321.14 151.64 64.93 54.24 214.15 216.84 160.03 89.08 481.31 165.1

8

344.8

3 172.41

(La/Yb)N 64.00 88.30 10.80 40.90 17.50 31.50 72.30 77.40 65.90 16.70 13.70 13.50 21.50

Eu/Eu* 0.35 0.47 0.74 1.93 2.05 0.61 0.95 1.07 2.19 0.71 0.81 0.66 1.05

K/Rb 1054.2 508.3 178.4 117.3 101.6 137.5 280.5 174.1 432.1 156.7 127.2 219.9 203.6

Sr/Y 43.6 15.9 23.8 123.5 91.6 36.1 126.0 86.6 138.1 8.0 26.1 12.8 35.9

Remark:A/CNK=mole [Al/(Ca+Na+K)] ; FeOT=0.8998*Fe2O3; LOI:Loss on ignition. (La/Yb)N=(La/0.310)/(Yb/0.209); Eu/Eu*=EuN/

(SmN+ GdN), N:Standardized values of chondrites


Continue Supplementary Table 1 The relevant parameters of major elements (wt.%) and trace elements

(ppm) in charnockites of NCC

Sample BQG

–5 BQG–6 BQG–7

BQG–

8

BQG–

9

BQG–

10

LYS–

1 LYS–2

LYS

–3

LYS–

4 LYS–5

LYS–

6

Rock BQG Charnockite LYS Charnockite

SiO2 57.37 66.89 67.59 59.56 72.19 70.03 59.65 63.44 62.36 68.08 59.56 65.55

TiO2 0.75 0.71 0.58 0.88 0.35 0.30 0.67 0.49 0.46 0.59 1.04 0.45

Al2O3 17.15 14.35 14.69 15.49 13.27 14.46 16.69 17.26 15.56 15.97 16.49 16.19

FeOT 7.14 4.89 3.50 7.45 2.26 2.81 5.36 3.98 4.74 2.76 6.98 4.79

MnO 0.11 0.04 0.03 0.11 0.02 0.05 0.03 0.03 0.06 0.03 0.09 0.05

MgO 3.31 1.94 1.55 3.34 1.18 1.30 3.37 2.50 3.66 1.21 3.47 2.10

CaO 4.77 1.52 1.62 4.65 1.30 2.08 5.60 3.37 5.28 3.48 5.83 3.98

Na2O 4.37 3.26 3.31 3.54 3.04 4.05 4.19 4.48 3.96 4.50 4.44 3.90

K2O 2.50 4.49 6.54 3.09 5.43 2.69 2.20 2.59 1.40 2.59 0.80 1.81

P2O5 0.44 0.58 0.23 0.58 0.16 0.22 0.27 0.38 0.16 0.14 0.23 0.04

LIO 1.57 1.55 0.55 1.01 0.55 1.49 1.05 0.72 1.62 0.12 0.02 0.35

Total 99.78 100.49 100.34 99.95 99.83 99.61 99.34 99.29 99.47 99.52 99.27 99.34

Na2O+K

2O 6.87 7.75 9.85 6.63 8.47 6.74 6.39 7.07 5.36 7.09 5.24 5.71

K2O/Na2

O 0.57 1.38 1.98 0.87 1.79 0.66 0.53 0.58 0.35 0.58 0.18 0.46

Mg# 45.20 41.40 44.10 44.40 48.20 45.20 52.80 52.80 57.90 43.90 47.00 43.90

A/CNK 0.92 1.10 0.95 0.88 1.00 1.08 0.86 1.06 0.88 0.96 0.88 1.04

Ba – – 650.0 635.0 – 841.0 812.0 1254.0 420.0 671.0 416.0 846.0

Cr – – – – – – 19.4 16.9 17.8 8.6 19.7 16.6

Sr – – 214.7 507.1 – 640.8 618.0 634.0 523.0 374.0 683.0 552.0

V – – – 102.0

0

95.00 86.00 58.00 135.00 85.00

Zr – – 174.2 153.2 – 115.1 120.0 60.0 102.0 161.0 121.0 83.0

Rb – – 101.9 90.1 – 66.7 49.3 65.9 22.4 43.9 3.0 36.0

U – – – – – – – – – – – –

Th – – – – – – <1 28.50 <1 <1 <1 <1

Ta – – – – – – <0.5 <0.5 <0.5 1.10 0.60 <0.5

Hf – – – – – – 4.20 2.30 3.20 5.30 3.60 2.70

Nb – – – – – – 8.00 5.90 6.50 10.70 8.90 7.00

La 44.72 109.40 119.50 63.80 122.80 26.64 27.39 – 24.44 19.24 21.33 20.67

Ce 79.19 211.02 199.50 114.09 158.20 43.28 58.13 – 54.32 30.59 47.34 29.93

Pr 9.43 24.31 20.54 12.88 19.77 5.35 7.94 – 7.53 3.46 6.22 3.12

Nd 33.85 83.68 68.16 44.40 61.74 18.61 33.29 – 29.27 11.85 24.18 9.99

Sm 6.04 13.15 9.70 7.61 8.41 2.94 6.41 – 5.49 1.99 4.11 1.31

Eu 1.46 1.70 1.57 1.44 1.09 0.85 1.23 – 1.14 1.11 0.96 1.59

Gd 4.95 10.29 7.25 6.22 5.91 2.42 5.05 – 4.18 1.55 3.00 0.95

Tb 0.69 1.57 0.98 0.88 0.81 0.34 0.65 – 0.55 0.20 0.40 0.13

Dy 3.68 7.61 5.44 4.59 4.20 1.85 3.23 – 2.76 1.00 2.05 0.71

Ho 0.81 1.68 1.22 1.06 0.75 0.40 0.59 – 0.53 0.19 0.40 0.16

Er 2.13 4.40 3.01 2.64 1.96 1.05 1.42 – 1.28 0.48 1.03 0.44

Tm 0.32 0.66 0.44 0.39 0.28 0.16 0.20 – 0.19 0.07 0.14 0.07

Yb 1.76 3.68 2.19 2.17 1.48 0.89 1.06 – 1.15 0.43 0.88 0.46

Lu 0.28 0.58 0.36 0.37 0.26 0.15 0.15 – 0.17 0.07 0.13 0.07

Y 19.72 38.98 25.28 23.78 15.59 9.36 13.75 – 12.42 4.53 9.45 3.67

∑REE 189.3

2 473.74 439.85 262.54 387.65 104.9

3

146.7

4 – 133.0

0 72.23 112.17 69.60

(La/Yb)

N 15.40 18.00 33.10 17.80 50.40 18.20 15.70 12.90 27.10 14.70 27.20

Eu/Eu* 0.82 0.45 0.58 0.65 0.48 0.99 0.67 – 0.73 1.94 0.84 4.39

K/Rb – – 266.4 142.4 – 167.4 185.2 163.1 259.4 244.9 1106.9 208.7

Sr/Y – – 8.5 21.3 – 68.5 44.9 – 42.1 82.6 72.3 150.4






Sample LYS–7 LYS–8 LYS–9 LYS–10 LYS–11 LYS–1

2

CKS–1 CKS–2 CKS–3 CKS–4 CKS–5 CKS–6 CKS–7

Rock LYS Charnockite CKS Charnockite

SiO2 62.32 52.21 56.61 70.26 67.23 62.28 57.54 57.76 47.34 63.52 59.47 55.80 68.74

TiO2 0.41 1.15 0.62 0.06 0.29 0.32 0.50 0.51 1.26 0.28 0.59 0.78 0.24

Al2O3 16.25 15.24 19.52 16.61 15.48 19.40 20.53 20.06 18.07 17.69 14.83 18.76 15.94

FeOT 5.98 10.08 5.17 1.68 2.85 3.28 3.59 3.77 10.06 3.84 7.52 5.34 2.00

MnO 0.09 0.22 0.12 0.06 0.08 0.07 0.05 0.06 0.10 0.07 0.10 0.09 0.04

MgO 3.67 6.05 3.19 2.41 1.69 2.24 1.77 1.68 5.21 1.80 3.54 3.34 1.24

CaO 5.11 7.84 7.47 4.33 4.27 5.94 4.19 3.34 8.74 4.63 5.07 5.58 3.06

Na2O 4.22 3.96 4.94 4.59 4.55 4.77 5.31 3.25 3.62 4.28 4.07 4.50 3.77

K2O 0.84 0.93 0.94 1.04 3.19 1.46 5.18 8.17 2.12 1.42 2.11 2.12 2.71

P2O5 0.24 0.47 0.22 0.01 0.16 0.20 0.21 0.21 0.60 0.13 0.24 0.46 0.16

LIO 0.01 0.50 0.42 0.37 0.21 0.07 0.88 1.50 2.53 1.71 1.88 2.26 2.96

Total 99.19 99.06 99.38 101.47 100.09 100.07 99.86 100.42 99.92 99.55 99.77 99.26 100.17

Na2O+K2O 5.06 4.89 5.88 5.63 7.74 6.23 10.49 11.42 5.74 5.70 6.18 6.62 6.48

K2O/Na2O 0.20 0.23 0.19 0.23 0.70 0.31 1.03 0.40 1.71 3.01 1.93 2.12 1.39

Mg# 52.20 51.70 52.40 71.90 51.40 54.90 0.47 0.44 0.48 0.46 0.46 0.53 0.49

A/CNK 0.95 0.70 0.86 1.00 0.83 0.96 0.93 0.99 0.75 1.04 0.81 0.94 1.08

Ba 241.0 253.0 247.0 – – – – – – – – – –

Cr 18.6 34.9 15.3 – – – – – – – – – –

Sr 735.0 376.0 644.0 – – – 627.0 691.0 1297.0 494.0 690.0 985.0 659.0

V 84.0 257.0 97.0 – – – – – – – – – –

Zr 119.0 66.0 35.0 – – – 269.0 376.0 94.1 138.0 102.0 132.0 120.0

Rb 9.10 15.80 11.6 – – – 121.0 141.0 38.0 40.3 31.6 31.4 37.0

U – – – – – – – – – – – – –

Th 2.10 1.40 <1 – – – 7.00 8.60 7.40 6.20 6.40 6.00 6.10

Ta <0.5 1.10 1.10 – – – – – – – – – –

Hf 4.00 2.40 2.10 – – – – – – – – – –

Nb 5.00 14.70 9.80 – – – 5.50 5.10 7.60 7.20 4.80 5.10 4.50

La 25.09 22.29 21.09 13.62 18.78 20.83 18.94 16.09 27.66 22.82 14.70 39.03 17.07

Ce 48.02 59.81 47.41 17.64 31.06 34.83 30.84 24.08 54.15 44.80 23.82 70.91 24.77

Pr 5.45 9.04 6.97 1.77 4.37 3.96 3.59 2.71 7.13 2.52 3.01 9.36 2.64

Nd 19.22 40.09 28.97 4.16 13.31 15.58 13.21 9.78 32.85 22.70 11.18 32.55 7.84

Sm 3.25 10.19 6.38 0.39 2.75 2.61 2.65 2.02 7.17 4.80 2.51 5.89 1.47

Eu 1.26 1.82 2.03 0.58 0.90 0.95 1.59 1.56 1.99 1.21 0.83 1.50 0.63

Gd 2.63 9.56 5.60 0.43 3.13 2.85 2.04 1.77 5.65 3.43 1.65 3.64 1.02

Tb 0.37 1.38 0.81 0.04 0.30 0.30 0.30 0.30 0.71 0.42 0.30 0.33 0.30

Dy 1.89 7.25 4.34 0.17 1.35 1.65 1.34 0.93 3.85 1.71 1.25 2.19 0.43

Ho 0.39 1.30 0.80 0.03 0.27 0.29 0.29 0.21 0.79 0.37 0.25 0.43 0.11

Er 1.02 3.12 1.92 0.07 0.38 0.48 0.66 0.42 1.89 1.30 0.64 1.12 0.12

Tm 0.17 0.45 0.28 0.01 0.10 0.10 0.10 0.13 0.26 0.20 0.10 0.14 0.10

Yb 1.05 2.43 1.54 0.08 0.39 0.41 0.65 0.49 1.50 1.10 0.61 0.87 0.23

Lu 0.17 0.33 0.22 0.02 0.10 0.10 0.10 0.12 0.24 0.18 0.10 0.14 0.10

Y 9.41 28.60 17.45 0.79 4.94 6.31 6.89 8.00 19.10 13.80 6.51 10.85 2.47

∑REE 109.98 169.06 128.36 39.01 77.19 84.94 76.30 60.61 145.84 107.56 60.95 168.10 56.83

(La/Yb)N 14.50 5.56 8.30 103.00 29.20 30.80 17.66 19.90 11.18 12.57 14.61 27.19 44.98

Eu/Eu* 1.33 0.57 1.04 4.36 0.94 1.07 2.10 2.54 0.96 0.92 1.25 1.00 1.58

K/Rb 383.2 244.3 336.4 – – – 177.4 240.0 231.6 146.3 277.2 280.3 304.0

Sr/Y 78.1 13.2 36.9 – – – 91.1 86.4 67.9 35.8 105.9 90.8 266.8






Sample CKS–8 CKS–9 CKS–10 CKS–11 CKS–12 CKS–13 CKS–

14

CKS–

15

XWL

BL–1

XWL

BL–2

XWL

BL–3

XWL

BL–4

XWL

BL–5

XWL

BL–6

Rock CKS Charnockite XWLBL Charnockite

SiO2 60.50 61.40 63.60 59.60 60.60 49.30 71.70 46.80 64.79 65.43 61.29 68.91 64.96 69.56

TiO2 0.86 0.65 0.40 0.85 0.54 0.83 0.22 0.47 0.50 0.48 0.58 0.35 0.65 0.39

Al2O3 15.20 15.27 15.27 17.45 16.06 13.45 14.86 16.29 15.75 19.19 14.03 16.09 16.16 15.52

FeOT 6.30 6.69 4.79 5.25 5.06 9.90 1.74 9.38 5.22 2.04 8.14 3.06 5.18 3.12

MnO 0.10 0.10 0.10 0.10 0.10 0.20 0.03 0.20 0.05 0.03 0.10 0.03 0.07 0.05

MgO 4.00 3.50 2.90 2.50 4.10 9.40 0.60 8.50 2.19 0.90 3.98 1.20 2.12 1.32

CaO 3.70 3.20 4.00 4.40 4.60 8.90 2.90 11.00 5.74 4.87 6.76 4.41 5.14 4.26

Na2O 4.50 4.10 3.90 4.90 3.80 2.90 5.10 2.30 4.22 5.38 3.46 4.28 4.14 4.45

K2O 1.90 2.10 2.40 2.40 2.20 2.30 1.60 2.20 0.66 0.66 0.52 0.78 0.95 0.81

P2O5 0.30 0.20 0.20 0.20 0.10 1.30 0.10 0.04 0.12 0.12 0.18 0.10 0.25 0.13

LIO 1.65 1.75 1.75 1.35 2.00 1.25 0.85 1.30 0.37 0.42 0.58 0.50 0.48 0.36

Total 99.16 99.27 99.38 99.25 99.38 99.95 99.63 99.15 99.61 99.52 99.62 99.70 100.1

0 99.96

Na2O+K2O 6.40 6.20 6.30 7.30 6.00 5.20 6.70 4.50 4.88 6.04 3.98 5.06 5.09 5.26

K2O/Na2O 2.37 1.95 1.63 2.04 1.73 1.26 3.19 1.05 6.39 8.15 6.65 5.49 4.36 5.49

Mg# 0.53 0.48 0.52 0.46 0.59 0.63 0.38 0.62 0.45 0.47 0.49 0.44 0.45 0.46

A/CNK 0.94 1.03 0.94 0.93 0.94 0.57 0.96 0.62 0.87 1.04 0.76 1.01 0.94 0.97

Ba 881.0 689.0 1112.0 1700.0 675.0 601.0 1244.

0 272.0 245.0 796.0 266.0 298.0 230.0 423.0

Cr 23.1 19.9 16.5 15.2 17.6 36.2 4.4 43.8 34.0 9.0 199.0 5.9 30.2 9.3

Sr 675.0 609.0 670.0 1099.0 597.0 493.0 1244.

0 272.0 270.0 437.0 217.0 258.0 225.0 299.0

V 143.0 154.0 79.0 93.0 102.0 238.0 22.0 172.0 16.5 16.6 20.1 14.8 18.7 15.3

Zr 105.0 99.0 136.0 126.0 71.0 62.0 89.0 35.0 136.0 248.0 107.0 72.9 182.0 160.0

Rb 27.6 35.0 48.4 39.0 54.4 70.30 18.50 44.60 3.88 5.20 4.74 4.85 4.44 3.66

U – – – – – – – – 0.04 0.11 0.05 0.03 0.08 0.08

Th 1.00 1.00 1.00 1.00 1.00 1.10 1.00 1.60 0.02 0.08 0.10 0.02 0.42 0.06

Ta <0.5 1.00 <0.5 <0.5 0.70 <0.5 <0.5 <0.5 0.20 0.17 0.21 0.07 0.31 0.21

Hf 3.10 3.00 4.30 3.80 2.60 2.40 3.30 1.20 3.30 5.70 2.90 1.85 4.93 4.10

Nb 9.30 8.10 4.40 8.40 5.00 5.20 3.30 3.80 4.40 3.27 5.17 2.32 6.67 3.29

La 25.78 23.22 18.48 40.89 14.21 10.32 16.90 12.79 11.00 9.82 14.30 10.30 15.80 10.20

Ce 47.65 38.05 33.82 73.78 27.68 23.22 25.96 22.35 23.50 16.30 33.10 16.90 31.70 18.80

Pr 5.88 4.54 4.07 8.75 3.53 3.60 2.63 2.97 3.01 1.65 4.40 1.79 3.87 2.03

Nd 21.81 16.09 14.53 32.66 13.55 14.82 8.20 9.86 12.20 5.53 19.00 5.75 15.00 7.12

Sm 3.43 2.39 2.45 4.65 2.30 3.30 0.91 1.96 2.79 0.97 4.39 0.91 3.02 1.30

Eu 1.21 1.13 1.26 1.83 0.85 1.09 1.12 0.63 0.87 1.03 1.00 0.66 0.91 0.82

Gd 2.63 1.71 1.89 3.12 1.84 3.43 0.67 2.14 2.70 0.78 4.14 0.72 2.69 1.08

Tb 0.34 0.24 0.25 0.38 0.25 0.50 0.08 0.36 0.42 0.10 0.69 0.09 0.38 0.16

Dy 1.77 1.16 1.34 1.88 1.26 3.00 0.40 2.32 2.43 0.53 4.06 0.45 2.12 0.91

Ho 0.33 0.22 0.25 0.34 0.25 0.62 0.08 0.49 0.49 0.10 0.79 0.08 0.40 0.18

Er 0.83 0.58 0.64 0.75 0.65 1.64 0.22 1.42 1.37 0.28 2.06 0.21 1.09 0.49

Tm 0.13 0.09 0.10 0.11 0.10 0.26 0.04 0.24 0.20 0.04 0.30 0.03 0.16 0.07

Yb 0.74 0.55 0.58 0.65 0.64 1.57 0.28 1.49 1.27 0.29 1.85 0.20 1.01 0.47

Lu 0.12 0.09 0.09 0.10 0.10 0.24 0.05 0.24 0.19 0.04 0.28 0.03 0.15 0.07

Y 7.87 5.05 5.25 7.74 6.08 14.23 2.23 12.18 12.80 3.22 19.80 2.57 10.90 5.24

∑REE 112.65 90.06 79.75 169.89 67.21 67.61 57.54 59.26 75.24 40.68 110.1

6 40.69 89.20 48.94

(La/Yb)N 21.11 25.59 19.31 38.13 13.46 3.98 36.58 5.20 6.16 24.56 5.52 37.08 11.22 15.72

Eu/Eu* 1.24 1.72 1.80 1.48 1.27 1.00 4.41 0.95 0.96 3.62 0.72 2.49 0.97 2.10

K/Rb 278.2 251.4 201.5 252.2 170.9 132.9 352.3 202.0 1412.

1

1053.

6 910.7 1335.

1

1776.

2 1837.2

Sr/Y 85.8 120.6 127.6 141.9 98.2 34.6 557.8 22.3 21.1 135.7 10.9 100.4 20.6 57.1






Sample XWLB

L–7

XWLB

L–8

XWLB

L–9

XWLB

L–10

XWLB

L–11

XWLB

L–12

XWL

BL–13

XWL

BL–14

XWLB

L–15

XWLB

L–16 JN–1 JN–2 JN–3 JN–4

Rock XWLBL Charnockite JN Charnockite

SiO2 67.56 70.66 69.58 71.43 70.73 63.08 62.35 59.65 62.36 59.44 56.86 62.45 54.85 55.55

TiO2 0.44 0.14 0.09 0.09 0.04 0.43 0.51 0.67 0.46 0.58 1.66 1.39 1.69 1.09

Al2O3 16.12 13.04 16.06 16.09 15.64 16.61 17.57 16.69 15.56 17.49 16.01 15.73 16.64 17.87

FeOT 3.54 3.76 2.34 1.67 2.05 5.27 4.38 5.36 4.74 5.31 8.60 6.23 9.26 7.50

MnO 0.05 0.04 0.03 0.02 0.02 0.07 0.07 0.03 0.06 0.06 0.10 0.06 0.12 0.12

MgO 1.69 1.64 1.15 0.91 1.22 3.47 2.63 3.37 3.66 3.24 2.51 0.97 3.16 3.38

CaO 5.43 2.00 4.03 4.00 4.09 5.25 5.07 5.60 5.28 5.89 5.69 3.78 5.80 6.73

Na2O 4.06 4.76 4.37 4.45 4.38 4.20 5.07 4.19 3.96 4.50 2.55 2.67 2.90 4.68

K2O 0.61 1.13 1.13 1.03 0.41 1.48 1.71 2.20 1.40 1.63 3.06 3.77 2.73 1.20

P2O5 0.09 0.07 0.09 0.06 0.03 0.22 0.26 0.27 0.16 0.34 0.48 0.41 0.77 0.56

LIO 0.34 1.90 1.06 0.38 0.76 0.92 1.52 1.05 1.62 0.76 1.16 1.86 0.99 0.75

Total 99.94 99.14 99.93 100.13 99.73 100.99 101.14 99.08 99.26 99.24 99.64 100.00 99.93 99.69

Na2O+K2O 4.67 5.89 5.50 5.48 4.79 5.68 6.78 6.39 5.36 6.13 0.90 1.03 0.91 5.88

K2O/Na2O 6.66 4.21 3.87 4.32 10.68 2.84 2.96 1.90 2.83 2.76 5.61 6.44 5.63 3.90

Mg# 0.49 0.46 0.49 0.52 0.54 0.57 0.54 0.55 0.60 0.55 0.37 0.24 0.40 0.47

A/CNK 0.94 1.03 1.02 1.02 1.04 0.92 0.90 0.86 0.88 0.88 0.90 1.02 0.91 0.84

Ba 206.0 336.0 484.0 397.0 201.0 637.0 194.0 812.0 420.0 651.0 1375.0 1555.0 1595.0 480.0

Cr 18.8 28.0 112.0 43.0 419.0 278.0 33.0 19.0 18.0 40.0 40.0 50.0 70.0 78.4

Sr 248. 407.0 542.0 686.0 331.0 639.0 943.0 618.0 523.0 578.0 422.0 448.0 764.0 576.0

V 14.6 – – – – – – – – – – – – –

Zr 129.0 65.0 59.0 56.0 48.0 140.0 117.0 120.0 102.0 160.0 390.0 400.0 360.0 200.0

Rb 2.6 10.0 11.0 5.0 3.0 48.0 12.0 49.0 22.0 35.0 77.4 90.9 59.5 11.0

U 0.04 0.17 0.04 0.05 0.05 0.15 0.15 0.40 0.30 0.26 0.14 0.27 0.15 0.19

Th 0.04 0.15 0.16 0.12 0.12 0.15 0.88 1.00 1.00 1.09 0.42 0.55 0.34 0.26

Ta 0.21 0.04 0.11 0.07 0.04 0.24 0.27 0.17 1.10 0.90 1.10 0.61

Hf 3.03 2.10 1.60 1.60 1.30 3.60 3.40 4.20 3.20 3.90 9.30 9.90 8.50 4.99

Nb 4.09 0.90 2.70 1.30 0.40 5.40 7.20 8.00 6.50 4.90 19.90 17.10 20.00 15.00

La 9.24 15.00 15.36 14.09 14.60 22.15 38.01 27.39 24.44 27.00 48.00 49.20 72.10 45.10

Ce 17.80 20.39 24.18 22.33 21.40 44.05 82.00 58.13 54.32 55.00 98.10 93.50 162.00 92.60

Pr 2.20 1.78 2.38 2.27 2.49 5.85 10.86 7.94 7.53 6.18 12.85 11.85 21.90 12.70

Nd 8.87 5.08 7.68 7.34 8.13 22.75 45.12 33.29 29.27 23.70 50.30 44.80 88.50 50.80

Sm 1.84 0.57 1.05 0.86 0.97 4.21 8.20 6.41 5.49 4.04 9.10 7.76 15.60 9.93

Eu 0.75 1.26 0.63 0.90 0.97 1.17 1.50 1.23 1.14 1.08 2.53 2.63 2.61 1.99

Gd 1.84 0.96 1.03 0.90 0.80 3.79 6.28 5.05 4.18 3.10 7.55 5.91 11.45 8.05

Tb 0.27 0.06 0.10 0.08 0.06 0.48 0.85 0.65 0.55 0.37 0.98 0.70 1.38 1.08

Dy 1.55 0.22 0.40 0.31 0.26 2.43 4.08 3.23 2.76 1.96 5.03 3.51 6.59 5.82

Ho 0.30 0.04 0.07 0.05 0.04 0.46 0.73 0.59 0.53 0.35 0.98 0.67 1.20 1.15

Er 0.84 0.12 0.16 0.13 0.12 1.16 1.76 1.42 1.28 1.04 2.69 1.84 3.01 3.05

Tm 0.12 0.02 0.02 0.02 0.02 0.16 0.24 0.20 0.19 0.14 0.37 0.25 0.40 0.48

Yb 0.75 0.16 0.15 0.14 0.14 1.09 1.46 1.06 1.15 0.84 2.35 1.56 2.42 3.12

Lu 0.11 0.03 0.02 0.02 0.02 0.17 0.20 0.15 0.17 0.13 0.34 0.25 0.34 0.48

Y 8.01 3.00 3.00 3.00 2.00 13.00 19.00 14.00 12.00 13.00 25.30 17.60 31.60 30.60

∑REE 54.49 48.69 56.23 52.44 52.02 122.92 220.29 160.74 145.00 137.93 247.17 224.43 389.50 236.3

5 (La/Yb)N 8.80 65.80 73.20 74.80 74.80 14.50 18.70 18.50 15.20 23.10 12.38 19.11 18.05 8.76

Eu/Eu* 1.24 5.20 1.80 3.10 3.40 0.90 0.60 0.70 0.70 0.90 0.94 1.19 0.60 0.68

K/Rb 1918.1 938.1 852.7 1710.1 1134.5 255.9 1182.9 372.7 528.3 386.6 328.2 344.3 380.9 905.6

Sr/Y 30.9 135.7 180.7 228.7 165.5 49.1 49.6 44.1 43.6 44.5 16.7 25.5 24.1 18.8






Sample JN–5 JN–6 JN–7 JN–8 JN–9 JN–10 GHY

–1

GHY–

2

GHY–

3

GHY

–4

GHY–

5

GHY

–6

GHY

–7

GHY–

8

Rock JN Charnockite GHY Charnockite

SiO2 62.67 63.70 69.99 70.20 71.17 71.79 65.78 57.52 55.01 60.56 65.03 68.28 66.58 61.59

TiO2 0.74 0.87 0.27 0.43 0.45 0.30 0.58 0.80 0.60 0.85 0.40 0.20 0.50 0.65

Al2O3 16.30 15.02 15.03 14.28 13.72 14.38 15.91 16.17 13.37 14.10 14.74 15.50 15.14 16.11

FeOT 4.83 5.60 2.49 3.11 2.59 1.69 2.95 6.23 3.79 8.37 3.80 2.28 4.35 5.08

MnO 0.07 0.09 0.02 0.05 0.04 0.02 0.03 0.10 0.09 0.13 0.04 0.24 0.06 0.07

MgO 1.85 1.91 0.20 1.17 0.77 0.32 1.82 4.76 6.15 3.99 1.76 3.53 2.32 3.61

CaO 4.43 3.11 1.29 2.67 1.90 1.25 3.98 6.04 9.15 5.52 4.09 0.66 3.17 4.18

Na2O 4.18 4.20 3.41 3.66 2.82 3.18 4.25 3.75 3.75 3.25 4.12 4.17 3.65 4.20

K2O 3.60 3.05 6.58 3.68 5.61 6.27 1.88 1.56 2.40 1.00 2.81 3.27 2.50 2.00

P2O5 0.46 0.55 0.07 0.17 0.16 0.10 0.16 0.22 0.12 0.12 0.25 0.10 0.15 0.30

LIO 0.42 1.94 0.57 0.30 0.75 0.75 1.38 0.89 2.40 1.52 1.21 1.44 1.04 0.89

Total 99.80 100.37 100.13 99.87 100.16 100.1 99.65 99.56 98.75 99.95 98.84 100.5

1 99.64 99.48

Na2O+K2O 7.78 7.25 9.99 7.34 8.43 9.45 6.13 5.31 6.15 4.25 6.93 7.44 6.15 6.20

K2O/Na2O 1.16 1.38 0.52 0.99 0.50 0.51 0.44 0.42 0.64 0.31 0.68 0.78 0.68 0.48

Mg# 0.43 0.40 0.14 0.43 0.37 0.27 0.48 0.57 0.72 0.46 0.43 0.69 0.47 0.54

A/CNK 0.86 0.95 1.00 0.96 0.97 1.00 0.98 0.86 0.53 0.86 0.85 1.33 1.04 0.97

Ba 997.0 792.0 1040.0 788.0 1670.0 1340 754.0 1039.0 551.0 952.0 1417.0 434.0 369.0 563.0

Cr 43.0 50.5 2.8 18.4 13.6 5.9 137.0 164.0 91.8 98.1 126.0 33.5 98.0 204.0

Sr 587.0 448.0 186.0 311.0 467.0 226.0 462.0 691.0 517.0 539.0 1081.0 678.0 512.0 756.0

V – – – – – – – – – – – – – –

Zr 234.0 313.0 400.0 205.0 290.0 188.0 94.3 110.0 101.0 133.0 120.0 60.8 47.7 95.4

Rb 87.6 65.9 186.0 85.5 126.0 160.0 37.3 82.8 41.1 48.2 32.9 12.6 12.3 11.7

U 0.31 0.36 0.72 0.25 0.66 0.21 – – – – – – – –

Th 0.33 2.17 15.80 1.02 132.00 1.38 0.43 0.41 3.11 0.99 0.27 0.32 0.57 0.17

Ta 1.15 1.87 0.04 0.23 0.16 0.46 0.34 0.34 0.69 0.47 0.39 0.53 0.30 0.35

Hf 8.55 8.19 9.64 5.34 7.55 4.98 3.14 3.68 3.23 4.22 4.01 2.03 1.59 3.18

Nb 16.30 23.60 2.24 6.84 5.96 8.53 4.64 6.79 6.39 5.10 5.08 2.36 2.51 5.93

La 47.20 61.90 59.90 34.20 110.00 32.80 20.30 26.00 31.60 21.80 32.50 8.49 10.90 25.80

Ce 102.00 137.00 102.00 58.90 176.00 52.70 35.90 46.00 54.00 38.60 66.10 13.30 18.00 53.50

Pr 13.20 18.60 10.20 6.38 16.50 5.63 4.64 5.62 6.46 4.67 9.03 1.61 2.19 7.63

Nd 53.80 79.70 34.40 23.70 53.30 19.30 18.90 21.60 23.70 18.60 37.20 6.39 8.59 33.40

Sm 10.10 16.70 4.86 3.93 6.17 2.80 3.52 3.27 3.78 3.55 6.46 1.24 1.55 6.67

Eu 2.25 2.43 1.36 1.30 2.03 1.53 1.21 1.47 1.22 1.31 1.94 0.85 0.95 1.84

Gd 7.73 14.10 3.15 2.89 4.13 2.19 3.07 2.83 3.18 3.52 4.73 1.10 1.57 5.12

Tb 1.03 2.18 0.40 0.35 0.43 0.24 0.43 0.35 0.39 0.61 0.62 0.17 0.25 0.74

Dy 5.29 12.30 1.65 1.62 1.67 1.11 2.19 1.60 1.75 3.55 2.55 0.97 1.45 3.54

Ho 1.03 2.25 0.26 0.31 0.31 0.22 0.45 0.34 0.31 0.73 0.47 0.20 0.32 0.69

Er 2.65 6.07 0.71 0.85 0.87 0.62 1.24 0.98 0.88 2.20 1.21 0.60 0.97 1.85

Tm 0.41 0.93 0.10 0.13 0.13 0.09 0.19 0.15 0.14 0.34 0.18 0.09 0.17 0.26

Yb 2.64 6.08 0.67 0.83 0.82 0.58 1.23 1.02 0.90 2.27 1.13 0.57 1.13 1.79

Lu 0.39 0.91 0.10 0.13 0.13 0.09 0.18 0.18 0.14 0.37 0.17 0.10 0.20 0.27

Y 29.00 58.80 6.33 9.61 10.40 6.75 11.30 7.91 8.90 17.80 11.40 4.90 8.10 16.80

∑REE 249.72 361.15 219.76 135.52 372.49 119.9 93.60 111.40 128.5

0

102.1

0 164.30 35.60 48.20 143.10

(La/Yb)N 10.84 6.17 54.18 24.97 81.30 34.27 11.13 17.19 23.59 6.47 19.39 10.06 6.50 9.72

Eu/Eu* 0.78 0.49 1.07 1.19 1.24 1.90 1.10 1.45 1.05 1.12 1.02 2.17 1.85 0.93

K/Rb 341.2 384.2 293.7 357.3 369.6 325.3 489.0 276.0 315.0 341.0 545.0 806.0 759.0 1003.0

Sr/Y 20.2 7.6 29.4 32.4 44.9 33.5 40.9 87.4 58.1 30.3 94.8 138.4 63.2 45.0






Sample GHY–

9

GHY–1

0

GHY–

11

GHY–1

2

GHY–1

3

GHY–

14

GHY

–15

GHY

–16

GHY–

17

GHY–

18

GHY

–19

GHY–

20

GHY

–21

GHY

–22

GHY–

23

GHY–

24

Rock GHY Charnockite

SiO2 63.78 62.37 66.52 64.10 57.89 63.66 63.78 63.13 62.58 63.73 58.30 60.74 61.51 59.27 59.49 56.95

TiO2 0.55 0.55 0.38 0.48 0.65 0.50 0.30 0.48 0.65 0.45 0.70 0.55 0.50 0.65 0.50 0.85

Al2O3 16.39 15.94 14.88 17.37 16.00 17.26 17.19 16.77 16.80 17.21 17.35 17.67 17.68 17.23 16.36 17.12

FeOT 4.20 4.42 3.40 3.07 4.95 3.66 3.34 4.10 4.43 3.31 5.33 4.02 3.59 4.94 4.75 5.48

MnO 0.05 0.06 0.06 0.05 0.11 0.03 0.04 0.06 0.07 0.06 0.06 0.06 0.04 0.09 0.08 0.09

MgO 3.83 3.10 1.58 1.93 3.26 1.63 1.67 2.07 2.23 1.59 2.78 2.82 2.25 3.63 3.36 3.86

CaO 2.01 3.90 3.41 4.55 5.49 2.94 4.34 5.17 5.10 4.56 5.78 5.44 5.22 6.62 6.13 5.96

Na2O 4.40 4.05 4.55 5.10 5.05 5.11 4.80 4.61 4.74 5.18 3.03 4.74 4.29 4.55 4.70 4.70

K2O 2.10 2.60 3.08 1.25 2.93 1.87 1.30 1.30 1.09 1.37 1.09 1.23 1.44 0.87 1.27 1.74

P2O5 0.15 0.22 0.16 0.14 0.34 0.20 0.12 0.16 0.20 0.14 0.20 0.12 0.20 0.10 0.14 0.44

LIO 1.11 1.22 0.70 0.92 0.56 2.03 2.61 1.10 0.98 1.21 2.83 0.68 1.36 0.40 0.97 0.75

Total 98.75 99.05 99.51 100.00 99.46 99.63 99.63 99.84 99.80 99.98 99.26 99.41 99.14 99.79 98.76 99.10

Na2O+K2O 6.50 6.65 7.63 6.35 7.98 6.98 6.10 5.91 5.83 6.55 4.12 5.97 5.73 5.42 5.97 6.44

K2O/Na2O 0.48 0.64 0.68 0.25 0.58 0.37 0.27 0.28 0.23 0.26 0.36 0.26 0.34 0.19 0.27 0.37

Mg# 0.60 0.54 0.42 0.49 0.52 0.41 0.44 0.45 0.45 0.43 0.47 0.53 0.50 0.55 0.54 0.55

A/CNK 1.24 0.96 0.87 0.96 0.74 1.09 1.00 0.91 0.92 0.94 1.04 0.93 0.98 0.84 0.81 0.84

Ba 600.0 620.0 501.7 626.3 1438.2 446.1 572.3 698.1 1128.9 1044.9 706.2 772.2 746.7 728.2 1270.1 1067.1

Cr 133.0 176.0 175.3 45.8 135.8 165.1 70.7 176.9 135.1 121.0 117.9 166.9 51.4 66.4 50.2 152.3

Sr 631.0 647.0 628.8 369.4 1101.0 480.2 363.9 762.3 755.5 657.9 690.7 788.6 680.1 364.8 873.9 663.3

V – – – – – – – – – – – – – – – –

Zr 116.0 113.0 124.2 162.6 133.8 88.5 159.0 131.6 152.6 114.1 86.0 103.7 65.9 114.2 800.0 171.1

Rb 17.7 35.2 12.8 33.1 20.7 6.3 22.3 21.3 49.6 62.1 18.9 12.7 10.0 24.3 93.4 82.4

U – – – – – – – – – – – – – – – –

Th 0.44 0.33 1.01 0.83 0.19 0.64 0.51 0.33 0.51 0.81 0.27 1.21 0.89 5.84 0.73 4.69

Ta 0.54 0.51 0.28 0.47 0.19 0.76 0.38 0.15 0.19 0.18 0.24 0.21 0.22 0.82 0.39 0.31

Hf 3.87 3.75 3.70 5.70 5.50 3.40 5.10 4.00 5.20 3.40 2.90 3.60 2.20 3.60 21.80 5.50

Nb 6.57 6.34 4.87 6.52 5.02 10.68 6.14 4.75 4.97 3.58 5.02 4.95 4.97 9.53 6.81 6.69

La 28.40 26.90 33.12 31.02 44.09 32.66 28.72 23.86 38.75 28.83 20.69 36.05 31.92 33.69 17.80 36.68

Ce 54.70 51.00 67.71 61.42 94.61 66.77 54.41 42.81 64.45 52.51 46.31 69.45 55.69 62.76 27.47 67.45

Pr 7.07 6.52 8.76 7.69 13.04 8.59 7.17 5.30 7.19 6.40 6.99 9.06 6.67 7.52 2.99 8.37

Nd 28.30 26.60 35.60 29.67 55.05 34.29 28.88 21.71 26.11 24.47 30.58 37.84 25.12 28.01 10.74 31.89

Sm 4.82 4.93 6.06 5.32 9.51 6.17 5.47 3.59 3.38 3.68 6.32 6.78 3.93 4.68 1.68 5.13

Eu 1.61 1.61 1.69 1.60 2.53 1.66 1.55 1.83 1.50 1.57 1.67 2.02 1.61 1.67 2.17 1.72

Gd 4.02 3.88 4.21 4.22 6.18 5.11 4.41 2.51 2.18 2.26 4.75 4.99 2.51 3.64 1.28 3.67

Tb 0.53 0.55 0.60 0.69 0.82 0.75 0.70 0.34 0.25 0.30 0.67 0.61 0.32 0.56 0.17 0.50

Dy 2.44 2.54 3.17 3.99 3.78 4.13 3.95 1.58 1.14 1.30 3.68 3.21 1.45 3.32 0.85 2.54

Ho 0.47 0.48 0.57 0.74 0.64 0.82 0.74 0.31 0.21 0.24 0.70 0.58 0.24 0.67 0.19 0.51

Er 1.36 1.42 1.52 2.19 1.79 2.30 2.08 0.83 0.56 0.71 1.83 1.53 0.64 2.01 0.60 1.44

Tm 0.22 0.21 0.23 0.33 0.23 0.34 0.31 0.13 0.07 0.10 0.28 0.21 0.08 0.36 0.11 0.22

Yb 1.31 1.36 1.51 2.23 1.54 2.43 2.06 0.83 0.50 0.74 1.92 1.40 0.63 2.31 0.75 1.55

Lu 0.20 0.21 0.23 0.33 0.22 0.36 0.29 0.12 0.08 0.12 0.27 0.20 0.09 0.35 0.14 0.23

Y 11.50 11.80 14.32 21.67 16.71 22.57 20.10 7.59 5.05 6.06 17.69 14.59 6.57 19.36 5.51 13.08

∑REE 135.40 128.20 165.00 151.40 234.00 166.40 140.7

0

105.7

0 146.40 123.20 126.7

0

173.9

0

130.9

0

151.5

0 66.90 161.90

(La/Yb)N 14.62 13.34 14.79 9.38 19.30 9.06 9.40 19.38 52.25 26.27 7.27 17.36 34.16 9.83 16.00 15.95

Eu/Eu* 1.09 1.09 0.97 1.00 0.95 0.88 0.93 1.78 1.59 1.54 0.90 1.02 1.47 1.20 4.34 1.16

K/Rb 554.0 345.0 610.0 511.0 791.0 1040.0 659.0 586.0 375.0 345.0 561.0 964.0 1060.

0 530.0 234.0 310.0

Sr/Y 54.9 54.8 43.9 17.1 65.9 21.3 18.1 100.4 149.6 108.6 39.0 54.1 103.5 18.8 158.6 50.7




Continue Supplementary Table 1The relevant parameters of major elements (wt.%) and trace elements


Sample GHY–2

5

GHY–

26

GHYH

–1

GHYH–

2

GHY

H–3

GHY

H–4

GHY

H–5

GHY

H–6

GHY

H–7

GHY

H–8

GHY

H–9

GHY

H–10

SAR

M–5

GBW

07104

ORE

AS1

05

Detecti–

onlimit

Rock GHY Hy–Tonalites

SiO2 62.63 57.85 71.29 69.44 68.46 72.47 69.35 70.73 71.79 72.01 69.22 69.55 51.07 0.01

TiO2 0.55 0.92 0.25 0.30 0.30 0.12 0.25 0.23 0.15 0.20 0.24 0.39 0.19 0.01

Al2O3 16.63 16.44 15.69 15.94 16.32 15.28 16.45 16.08 15.96 14.85 15.87 15.69 4.22 0.01

FeOT 3.69 4.68 1.47 1.89 1.86 1.92 2.21 1.67 1.25 1.90 2.20 1.97 12.77 0.01

MnO 0.05 0.08 0.01 0.05 0.04 0.02 0.02 0.04 0.04 0.04 0.05 0.06 0.23 0.01

MgO 2.28 3.12 0.77 0.89 0.89 0.53 0.77 0.59 0.28 0.58 0.94 0.44 25.4 0.01

CaO 5.16 5.66 4.54 4.86 5.07 2.41 2.54 4.16 2.95 2.29 2.98 3.09 2.60 0.01

Na2O 4.48 4.18 3.48 3.44 3.44 4.45 5.52 4.55 5.15 4.52 4.71 4.79 0.40 0.01

K2O 1.98 2.53 1.50 1.52 1.60 1.88 1.22 1.39 1.19 2.79 2.53 1.51 0.09 0.01

P2O5 0.20 0.38 0.07 0.12 0.10 0.03 0.06 0.10 0.06 0.07 0.08 0.11 0.01 0.01

LIO 0.83 1.75 0.64 0.99 0.94 0.82 1.09 0.58 0.82 0.56 0.80 0.60 4.48 0.01

Total 99.39 99.40 99.90 99.58 99.57 99.66 99.40 99.77 99.63 99.61 99.66 99.81

Na2O+K2O 6.46 6.71 4.98 4.96 5.04 6.33 6.74 5.94 6.34 7.31 7.24 6.30

K2O/Na2O 0.44 0.61 0.43 0.44 0.47 0.42 0.22 0.31 0.23 0.62 0.54 0.32

Mg# 0.50 0.53 0.39 0.39 0.39 0.27 0.33 0.31 0.21 0.29 0.38 0.23

A/CNK 0.88 0.82 1.00 0.99 0.98 1.11 1.09 0.97 1.05 1.01 1.00 1.04

Ba 1815.5 982.0 424.0 666.0 668.0 451.9 329.9 473.0 1737.

1

1235.

7

609.8 961.0 689 0.5

Cr 44.0 126.0 32.0 14.6 14.3 22.6 24.0 22.7 29.1 35.4 20.0 28.1 50

10

10

Sr 224.7 438.0 408.0 714.0 708.0 459.9 886.6 635.7 1049.

0

933.2 386.0 867.0 90.5 0.1

V – – – – – – – – – – – – 28 5

Zr 351.8 136.0 106.0 95.3 107.0 112.0 368.9 75.5 63.7 98.4 130.4 58.2 237 2

Rb 90.7 114.0 17.8 12.4 12.9 12.0 15.6 8.2 30.5 45.5 16.7 17.2 104.

0

0.2

U – – – – – – – – – – – – 528 0.05

Th 4.17 0.92 0.70 0.38 0.31 <3 17.16 0.19 0.42 3.71 0.18 0.11 376 0.05

Ta 0.30 0.42 0.19 0.16 0.09 – 0.20 0.25 0.23 0.10 0.19 0.42 4.5 0.1

Hf 10.40 4.53 3.70 3.50 3.90 – 11.00 2.40 2.20 3.10 4.10 1.94 6.1 0.2

Nb 11.76 5.87 2.70 2.19 1.70 <2 3.31 2.07 2.22 2.60 3.29 1.87 41.2 0.2

La 27.37 26.80 19.95 10.83 10.54 8.16 46.05 11.56 18.26 26.05 20.61 9.42 49.2 0.5

Ce 50.15 45.10 34.77 16.99 17.45 12.82 66.06 18.62 30.25 43.06 33.77 15.30 113.

0

0.5

Pr 6.32 5.28 4.28 1.91 2.06 1.76 6.53 1.85 3.46 4.92 3.98 2.05 15.4

5

0.03

Nd 25.47 20.20 16.31 6.23 6.55 5.54 21.63 6.52 13.13 17.28 14.09 7.79 62.9 0.1

Sm 4.44 3.30 2.93 0.92 1.03 1.00 2.56 0.87 2.06 2.47 2.07 1.30 15.5

0

0.03

Eu 1.98 1.28 0.76 0.59 0.57 0.54 1.59 0.98 1.17 1.04 1.24 0.61 1.53 0.03

Gd 3.78 3.03 2.53 0.61 0.68 0.90 1.70 0.56 1.38 1.56 1.45 1.01 12.6

0

0.05

Tb 0.56 0.41 0.30 0.07 0.08 0.11 0.24 0.07 0.17 0.22 0.19 0.12 2.11 0.01

Dy 3.35 2.16 1.43 0.32 0.40 0.36 1.08 0.35 0.82 1.16 0.83 0.51 12.2

0

0.05

Ho 0.75 0.45 0.24 0.07 0.09 0.07 0.20 0.07 0.15 0.20 0.15 0.09 2.54 0.01

Er 2.23 1.32 0.56 0.17 0.21 0.14 0.57 0.20 0.40 0.62 0.42 0.23 7.18 0.03

Tm 0.36 0.21 0.08 0.03 0.03 0.02 0.09 0.03 0.06 0.08 0.06 0.03 1.10 0.01

Yb 2.56 1.46 0.42 0.16 0.19 0.15 0.58 0.21 0.36 0.56 0.42 0.20 7.34 0.03

Lu 0.40 0.25 0.07 0.03 0.03 0.03 0.11 0.04 0.05 0.09 0.06 0.04 0.99 0.01

Y 21.60 11.90 5.63 1.53 1.84 1.67 5.13 1.76 3.77 5.82 3.88 2.01 64.9 0.5

∑REE 129.70 111.30 84.60 38.90 39.90 31.60 149.0

0

41.90 71.70 99.30 79.30 38.70

(La/Yb)N 7.21 12.38 32.02 45.63 37.40 36.68 53.53 37.11 34.20 31.36 33.08 31.29

Eu/Eu* 1.45 1.22 0.83 2.27 1.96 1.71 2.19 4.03 2.00 1.51 2.07 1.57

K/Rb 481.0 250.0 699.6 1017.6 1029.6 844.0 735.4 1396.9 322.9 508.3 1255.

4

728.8

Sr/Y 10.4 36.81 72.5 466.7 384.8 275.4 172.8 361.2 278.3 160.3 99.5 431.3




Geochemical characteristic of charnockite in North margin of ......LYS Charnockite), Guyang (BQG...

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Transcript of Geochemical characteristic of charnockite in North margin of ......LYS Charnockite), Guyang (BQG...