Geochronology and geochemistry of Late Devonian-Carboniferous igneous rocks in the Songnen-Zhangguangcai Range Massif, NE China: Constraints on the late Paleozoic tectonic evolution of the eastern Central Asian Orogenic Belt

Accepted Manuscript Geochronology and geochemistry of late Devonian-carboniferous igneous rocks in the Songnen-Zhangguangcai range massif, NE China: Constraints on the late Paleozoic tectonic evolution of the eastern central Asian Orogenic Belt

Peng Guo, Wen-Liang Xu, Zhi-Wei Wang, Feng Wang, Jin-Peng Luan PII: DOI: Reference:

S1342-937X(18)30034-0 https://doi.org/10.1016/j.gr.2018.01.007 GR 1911

To appear in: Received date: Revised date: Accepted date:

11 August 2017 30 December 2017 8 January 2018

Please cite this article as: Peng Guo, Wen-Liang Xu, Zhi-Wei Wang, Feng Wang, JinPeng Luan , Geochronology and geochemistry of late Devonian-carboniferous igneous rocks in the Songnen-Zhangguangcai range massif, NE China: Constraints on the late Paleozoic tectonic evolution of the eastern central Asian Orogenic Belt. The address for the corresponding author was captured as affiliation for all authors. Please check if appropriate. Gr(2018), https://doi.org/10.1016/j.gr.2018.01.007

This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.

ACCEPTED MANUSCRIPT Geochronology and geochemistry of Late Devonian–Carboniferous igneous rocks in the Songnen–Zhangguangcai Range Massif, NE China: constraints on the late Paleozoic tectonic evolution of the

PT

eastern Central Asian Orogenic Belt

RI

Peng Guoa, Wen-Liang Xua,b*, Zhi-Wei Wanga, Feng Wanga, Jin-Peng Luana College of Earth Sciences, Jilin University, Changchun 130061, China

b

Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of

SC

a

MA

NU

Land and Resources of China, Changchun 130061, China

Corresponding author: [email protected] (W. Xu) E–mail addresses: [email protected] (P. Guo); [email protected](W. Xu);

D

[email protected] (Z. W); [email protected] (F. Wang);

PT E

[email protected] (J. Luan) Postal address: 2199 Jianshe Street, College of Earth Sciences, Jilin University,

AC

CE

Changchun 130061, China

ACCEPTED MANUSCRIPT Abstract This paper presents new zircon U–Pb ages and Hf isotopic data, and whole–rock geochemical data for Late Devonian–Carboniferous igneous rocks from the Songnen–Zhangguangcai Range Massif (SRM), NE China, to constrain the late

PT

Paleozoic tectonic evolution of the eastern Central Asian Orogenic Belt and the nature

RI

of the crust beneath the SRM. LA–ICP–MS zircon U–Pb dating reveals two stages of

SC

magmatism in the Late Devonian (366 Ma) and Carboniferous (325–313 Ma). The Late Devonian magmatic event produced alkali feldspar granites with high SiO2 and

NU

total alkali contents, as well as pronounced negative Eu anomalies, similar to A-type

MA

granites. Based on these features, their high zircon εHf(t) values (+9.6 to +13.0), and the early Paleozoic tectonic evolution of the eastern SRM, we conclude that the

D

primary magma for the Late Devonian granites was generated by partial melting of

PT E

juvenile lower crust in a post-collisional extensional environment. The Carboniferous magmatic event produced a suite of intermediate–felsic igneous rocks. The

CE

intermediate rocks, including basaltic andesite, andesite, and quartz monzodiorites,

AC

have low SiO2 contents, high Mg#, high Cr, Co, and Ni contents, and display arc-like trace element characteristics. Based on these observations and their high zircon εHf(t) values (+5.8 to +10.7), we suggest their primary magma was derived from partial melting of depleted mantle, metasomatized by subduction-related fluids. The felsic rhyolites and monzogranites have high SiO2 contents, low Mg#, extremely low Cr, Co, and Ni contents, and zircon εHf(t) values of +10.5 to +13.7 and +4.2 to +6.9, respectively. These results indicate that the primary magma for the felsic rocks was

ACCEPTED MANUSCRIPT derived from partial melting of heterogeneous juvenile crust. The Carboniferous igneous rock assemblages, together with coeval carbonate sedimentary formations, record an intra-plate extensional setting. The zircon εHf(t) data of Paleozoic igneous rocks from the eastern SRM define a temporal trend that is consistent with tectonic

PT

evolution. The increase in εHf(t) values during the early late Paleozoic age mirrors

RI

changes in magma source, corresponding to a switch from subduction–collision to

SC

post-collision tectonic regimes in the SRM. The zircon Hf isotopic compositions of the studied Late Devonian–Carboniferous igneous rocks record crustal accretion in

NU

the eastern SRM during the Neoproterozoic–early Paleozoic. Reworking of these

MA

crustal materials occurred in a post-collisional extensional environment during the late Paleozoic.

D

Keywords: Songnen–Zhangguangcai Range Massif; Central Asian Orogenic Belt;

CE

1. Introduction

PT E

late Paleozoic; igneous rocks; Geochemistry

The Central Asian Orogenic Belt (CAOB), located between the Siberian and

AC

Tarim–North China cratons (Fig. 1a), is recognized as the world’s largest Phanerozoic accretionary orogenic collage (e.g., Sengör et al., 1993; Jahn, 2004; Windley et al., 2007; Safonova and Santosh, 2014; Xiao et al., 2015). Northeast (NE) China is located in the easternmost segment of the CAOB and includes, from west to east, the Erguna, Xing’an, Songnen–Zhangguangcai Range, Jiamusi, and Khanka massifs (Li, 2006). The formation and tectonic evolution of NE China followed the subduction of the Paleo-Asian Ocean (PAO) and the amalgamation of several micro-continental

ACCEPTED MANUSCRIPT massifs (Liu et al., 2017). Therefore, understanding the timing of closure of the PAO and the amalgamation of micro-continental massifs is crucial in constraining the tectonic evolution of the region. Numerous studies have focused on the final closure of the PAO along the Solonker–XarMoron–Changchun–Yanji suture zone (Fig. 1b), but the timing of closure remains poorly constrained to the period between the Late

PT

Permian and Early Triassic (e.g., Xiao et al., 2003, 2015; Li, 2006; Chen et al., 2009;

RI

Jian et al., 2010; Cao et al., 2013; Li et al., 2016) or the pre-Permian (e.g., Xu et al.,

SC

2013a, 2015). However, less attention has been paid to the time of closure amongst micro-continental massifs along the northern branches of the PAO, especially the

NU

branch between the Songnen–Zhangguangcai Range Massif (SRM) and Jiamusi Massif (JM; Zhou et al., 2009; Meng et al., 2010; Wang et al., 2012a, 2016; Xu et al.,

MA

2012). Consequently, the timing of amalgamation of these two massifs remains controversial. One hypothesis suggests that amalgamation occurred in the early

D

Paleozoic, based on early Paleozoic igneous rocks (Wang et al., 2012a, 2016) and

PT E

detrital zircon geochronology (Meng et al., 2010). However, others argue that an ocean existed between the SRM and JM in the Permian to Jurassic (Zhou et al., 2009;

CE

Zhu et al., 2015, 2017; Ge et al., 2016), and that their subsequent suturing along the N–S-trending Heilongjiang Complex occurred in the Early–Middle Jurassic (Wu et al.,

AC

2007; Zhou et al., 2009) or after the Late Jurassic (Zhu et al., 2015, 2017). These conflicting opinions are, to a large extent, the consequence of a limited understanding of the late Paleozoic evolution of these two massifs. The CAOB is renowned for the generation of large quantities of juvenile continent crust (e.g., Chen et al., 2000; Jahn et al., 2000; Wu et al., 2000, 2003; Jahn, 2004). However, the extent of juvenile crust in the CAOB has recently been challenged by Kröner et al. (2014), who argued that the history of the belt extends to

ACCEPTED MANUSCRIPT the Mesoproterozic and that the most voluminous Phanerozoic granites were derived from reworking of these rocks. This view was further verified by Wang et al (2016, 2017) in the eastern SRM, who suggested reworking of Meso- to Paleo-proterozoic crustal materials was responsible for the generation of early Paleozoic igneous rocks. In contrast, Jurassic granites from the same region are mainly fractionated and have

PT

I-type affinities that resulted from melting of juvenile crust (Wu et al., 2003). Thus,

RI

more geochemical and isotopic data, especially from the late Paleozoic igneous rocks,

SC

are needed to better constrain the processes of crustal growth and reworking beneath the SRM.

NU

In this paper, we present new zircon U–Pb ages, whole-rock geochemical and zircon Lu–Hf isotopic data from Late Devonian–Carboniferous igneous rocks of the

MA

eastern SRM. These new data constrain the tectonic evolution of the eastern CAOB

D

and the nature and evolution of the crust underlying the SRM.

PT E

2. Geological background and sample descriptions The SRM comprises the Songliao Basin, the Lesser Xing’an Range, and the

CE

Zhangguangcai Range. Borehole data reveal that the basement beneath the Songliao Basin is composed mainly of Paleozoic–Mesozoic granitoids and Paleozoic strata

AC

(Gao et al., 2007), along with minor ~1.8 Ga Paleoproterozoic meta-igneous rocks (Wang et al., 2006; Pei et al., 2007). The Lesser Xing’an and Zhangguangcai ranges contain intrusive rocks including Neoproterozoic–Paleozoic granitoids that were emplaced at 917–911, 841, 516–490, 482–450, 435–420 and 256–252 Ma, as well as voluminous Mesozoic granitoids (Wu et al., 2011; Wang et al., 2012a, 2016, 2017; Yu et al., 2013; Luan et al., 2017). In contrast, the well-documented Precambrian and Paleozoic supracrustal successions occur as remnants in a “sea” of granitoids (Meng

ACCEPTED MANUSCRIPT et al., 2010, 2011; Wang et al., 2014), and minor late Mesozoic volcanic and sedimentary strata overlie the granitoids (Xu et al., 2013b). The Zhangguangcailing Complex, previously thought to be Precambrian in age, has been shown to be a tectonic mélange containing early Paleozoic to early Mesozoic terranes (Wang et al., 2012b).

PT

The JM, separated from the SRM by the Jiayin–Mudanjiang Fault to the west

RI

(Fig. 1b), is dominated by voluminous Paleozoic granitoids and the Mashan Complex

SC

as well as minor amounts of Neoproterozoic granitoids and late Paleozoic and Mesozoic volcanic-sedimentary rocks (Cao et al., 1992; Wilde et al., 2000, 2003; Wu

NU

et al., 2011; Bi et al., 2014; Yang et al., 2014, 2017). The Paleozoic intrusive rocks within the JM were emplaced between the Cambrian and Early Ordovician (540–484

MA

Ma), and in the Permian (299–254 Ma) (Wilde et al., 2003; Wu et al., 2011; Bi et al., 2014, 2017; Yang et al., 2014, 2017; Dong et al., 2017). The Mashan Complex

D

recorded granulite facies metamorphism at ~560 and 500 Ma (Wilde et al., 1997,

PT E

2000; Yang et al., 2017).

Between the SRM and JM is the Heilongjiang Complex. Exposed along the

CE

Jiayin–Mudanjiang Fault, the complex consists of serpentinite, blueschist, greenschist, marble, amphibolite, muscovite–albite schist, and quartzite. It was overprinted by

AC

intense compressional deformation during the Early Jurassic (Li et al., 1999; Wu et al., 2007; Zhou et al., 2009) and was thought to represent a N–S trending suture belt between the SRM and JM (Cao et al., 1992; Wu et al., 2007; Zhu et al., 2015). The present study was carried out in the Zhangguangcai Range in the southeastern

SRM

and

focused

on

several

representative

Late

Devonian–Carboniferous intrusions and volcanic rocks. Sampling locations and mineral compositions of igneous rocks are presented in Table 1, and representative

ACCEPTED MANUSCRIPT photomicrographs are shown in Fig. 2. Note that sample numbers (e.g., 15XH2) represent locations, and if more than one sample was collected from a given location, samples are labeled sequentially (e.g., 15XH2-1). The petrographic characteristics of the samples are briefly described below. Sample 15XH2, an alkali feldspar granite, was collected from the Yanshou

PT

Pluton at a site located ~3 km northwest of Yanshou City (Fig. 1c). The sample is

RI

pink, medium-grained (Fig. 2b), has a massive structure, and contains alkali feldspar

SC

(~55%), quartz (~35%), plagioclase (5%), biotite (~3%) and accessory minerals (~2%) including zircon and apatite.

NU

Sample 15XH12, a monzogranite, was collected from the Yuejin Pluton (Fig. 1c). It displays a medium-grained massive structure (Figs. 2c and 2d), and contains quartz

MA

(~35%), alkali feldspar (~30%), plagioclase (~30%), biotite (~3%) and accessory minerals (~2%) including zircon, magnetite and apatite.

D

Samples 15XH19, 16XH1, and 16XH2 are quartz monzodiorites collected from

PT E

the Wulidicun Pluton (Fig. 1c). These samples exhibit medium-grained textures (Figs. 2e and 2f), and have a massive structure, and contain plagioclase (45–50%), alkali

CE

feldspar (20–25%), quartz (5–15%), biotite (5–10%), hornblende (5–10%) and accessory minerals including zircon and apatite.

AC

Samples 15XH18 and 16XH4 were collected from rocks mapped previously as the early Devonian Heilonggong Formation at a site located ~10 km north of Hengdaohezi town (Fig. 1c). The Heilonggong Formation is a suite of intermediate to felsic volcanic rocks, including basaltic andesite (15XH18-3; Fig. 2i), andesite (15XH18-1; Fig. 2h), dacite (15XH18-4, 15XH18-6; Fig. 2j), and rhyolite (16XH4; Fig. 2k). The basaltic andesite and andesite are dark grey, porphyritic, massive, and contain plagioclase phenocrysts (making up ~10% of the rock by volume) hosted in a

ACCEPTED MANUSCRIPT groundmass of plagioclase, clinopyroxene, and magnetite. The dacites are also dark grey, porphyritic, and massive. The phenocrysts (~15 %) consist of plagioclase (~10%) and quartz (~5%), and the groundmass (85%) is composed of felsic microcrystals and magnetite. The rhyolites exhibit porphyritic textures and have a rhyolitic structure. The phenocrysts (~45%) consist of quartz (~15%), alkali feldspar (~25%) and

PT

plagioclase (~5%), and the groundmass (55%) is composed of aphanitic felsic

RI

minerals.

SC

Sample HDY3, a rhyolite with a zircon U–Pb age of 317±2 Ma (Wang et al., 2012b), was collected from rocks previously mapped as the Zhangguangcailing

NU

Complex at a site located ~10 km northwest of Diaoyutai village (Fig. 1c). The sample is dark grey, porphyritic, massive, and contains quartz phenocrysts (~10%) in

MA

a groundmass of aphanitic felsic minerals. Six samples collected from this location

PT E

3. Analytical methods

D

were selected for geochemical analyses.

3.1 Zircon U–Pb dating

CE

Zircon grains were separated from whole-rock samples using the conventional heavy liquid and magnetic techniques, and then by handpicking under a binocular

AC

microscope. Laser ablation inductively coupled plasma mass spectrometry (LA–ICP–MS) zircon U–Pb analyses were performed using an Agilent 7500a ICP–MS equipped with a 193 nm laser, housed at the Geological Laboratory Centre, China University of Geosciences, Beijing, and the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan, China. A zircon 91500 was used as an external standard for age calibration, and the NIST SRM610 silicate glass was applied for instrument optimization. The

ACCEPTED MANUSCRIPT crater diameter was 36 and 32 μm during the analyses in these two Laboratories, respectively. The instrument parameter and detail procedures were described by Liu et al. (2010). The GLITTER (ver. 4.4, Macquarie University), ICPMSDataCal (Liu et al., 2010) and Isoplot (Ver. 3.0; Ludwig, 2003) programs were used for data reduction. Correction for common Pb was made following Anderson (2002). All LA–ICP–MS

PT

zircon isotope ratio and age uncertainties are quoted at the 1 sigma level, and are

RI

provided in Supplementary Table 1.

SC

3.2 Major and trace element determinations

For geochemical analysis, 27 whole-rock samples, after the removal of altered

NU

surfaces, were crushed in an agate mill to ~200 meshes. Whole-rock major and trace element compositions of the samples analyzed during this study were determined at

MA

the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan. Major element compositions were determined by

D

X-ray fluorescence (XRF; Rigaku RIX 2100 spectrometer) using fused-glass disks.

PT E

Trace element compositions were analyzed by ICP–MS (Agilent 7500a with a shield torch) after acid digestion of samples in Teflon bombs. The detailed procedures are

CE

the same as descriptions by Liu et al. (2008). Analytical uncertainties are in the range 1%–3%. The analytical results for the BHVO-1 (basalt), BCR-2 (basalt), and AGV-1

AC

(andesite) standards indicate that the analytical precision for major elements is better than 5%, and for trace elements, generally better than 10% (Rudnick et al., 2004). The results of analyses for major and trace elements are presented in Supplementary Table 2. 3.3 Hf isotope analyses In situ zircon Hf isotope analyses were undertaken using a Neptune Plus MC–ICP–MS in combination with a Geolas 2005 excimerArF laser ablation system

ACCEPTED MANUSCRIPT (193 nm) that was hosted at the state Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan. All data were acquired on zircon grain in single spot ablation mode with a spot size of 44 μm. The details of the operating conditions for the laser ablation system and the MC–ICP–MS instrument as well as the analytical method can refer to Hu et al. (2012). Present-day 176

Hf/177Hf = 0.282772 and

176

Lu/177Hf = 0.0332 (Blichert-Toft

PT

chondritic ratios of

RI

and Albarède, 1997) were used to calculate εHf(t) values, and Hf model ages were

SC

calculated using the methods of Griffin et al. (2002). The results of Lu-Hf isotope

NU

analyses are presented in Supplementary Table 3.

MA

4. Results 4.1 Zircon U–Pb dating

Zircons selected for U–Pb analysis are euhedral–subhedral, display striped

PT E

D

absorption or oscillatory growth zoning in CL images (Fig. 3), and have Th/U ratios of 0.22–1.51. Taken together, these properties indicate that these zircons are of magmatic origin (Pupin,1980; Koschek, 1993). Zircon U–Pb concordia diagrams are

CE

presented in Fig. 4. Where multiple groups of concordant ages were obtained, the

AC

youngest age was considered to represent the crystallization age of the magma, with the older ages representing captured zircons. For sample 15XH2-1, an alkali feldspar granite from the Yanshou Pluton, 20 analyses yield three groups of concordant

206

Pb/238U ages: 366 ± 5 Ma (mean square

weighted deviation (MSWD) = 0.29, n = 6), 393 ± 4 Ma (MSWD = 0.48, n = 8), and 414 ± 5 Ma (MSWD = 0.19, n =6) (Fig. 4a). The youngest age (366 Ma) is considered to represent the timing of crystallization of the alkali feldspar granite (i.e., Late Devonian), in contrast to the previously inferred age of late Variscan (HBGMR,

ACCEPTED MANUSCRIPT 1993). In sample 15XH12-1 (a monzogranite) from the Yuejin Pluton, 20 zircon grains were measured, and 11 analyzed zircons produced concordant ages (Fig. 4b). Excluding the discordant analyses, 11 analyses yield a weighted mean

206

Pb/238U age

of 313 ± 3 Ma (MSWD = 0.28), which is interpreted to represent the crystallization

PT

age of the monzogranite (i.e., Carboniferous), in contrast to the previously inferred

RI

age of early Paleozoic (HBGMR, 1993).

SC

Samples 15XH18-1 (andesite) and 16XH4-1 (rhyolite) were collected from the Heilongong Formation. Nineteen zircon grains were measured in sample 15XH18-1,

NU

yielding two groups of concordant ages at 315 ± 3 Ma (MSWD = 0.18, n= 16) and 343 ± 5 Ma (MSWD = 0.15, n =2), as well as a single–zircon age of 360 ± 5 Ma (Fig.

MA

4c). For sample 16XH4-1, the 206Pb/238U ages of 30 analytical spots yield two groups of concordant ages at 316 ± 2 Ma (MSWD = 0.34, n= 25) and 328 ± 5 Ma (MSWD =

D

0.15, n =4), as well as a single-zircon age of 342 ± 6 Ma (Fig. 4g). The youngest age

PT E

of ~316 Ma is considered to represent the timing of eruption of this suite of volcanic rocks (i.e., Carboniferous) in contrast to the previously inferred age of Early

CE

Devonian (HBGMR, 1993).

Samples 15XH19-1, 16XH1-1, and 16XH2-1 are quartz monzodiorites collected

AC

from the Wulidicun Pluton. Nineteen analytical spots for sample 15XH19-1 yield two groups of concordant 206Pb/238U ages at 325 ± 3 Ma (MSWD = 0.25, n = 17) and 344 ± 5 Ma (MSWD = 0.11, n = 2) (Fig. 4d). For sample 16XH1-1, 23 analytical spots yield a weighted mean

206

Pb/238U age of 324 ± 2 Ma (MSWD = 0.19; Fig. 4e). For

sample 16XH2-1, 20 analytical spots yield a weighted mean 206Pb/238U age of 321 ± 2 Ma (MSWD = 0.18; Fig. 4f). The concordant ages of ~325 Ma are interpreted to represent the crystallization age of the quartz monzogranites. Therefore, the

ACCEPTED MANUSCRIPT Wulidicun Pluton was emplaced in the Carboniferous, and not during late Variscan as previously thought (HBGMR, 1993). The

above

zircon

U–Pb

ages,

together

with

previously

published

geochronological data (Wang et al., 2012b), show that late Paleozoic magmatism in the eastern margin of the SZM can be subdivided into two main stages, during the

PT

Late Devonian (~366 Ma) and Carboniferous (313–325 Ma). The former are mainly

RI

alkali feldspar granites, and the latter consist of a suite of intermediate to felsic

4.2 Major and trace element geochemistry

NU

4.2.1 Late Devonian intrusive rocks

SC

igneous rocks.

The Late Devonian alkali feldspar granites have a restricted range of SiO2

MA

contents (72.35–73.72 wt.%), and are enriched in total alkalis (K2O + Na2O = 9.86–10.37 wt.%) with high K2O contents relative to Na2O (K2O/Na2O = 1.10–1.15).

D

In the total alkalis versus SiO2 (TAS) diagram of Irvine and Baragar (1971), these

PT E

rocks plot close to the boundary between the alkaline and subalkaline series (Fig. 5a). Their A/CNK [molar Al2O3/(CaO + K2O + Na2O)] values are 1.00–1.02, indicating a

CE

weakly peraluminous composition (Fig. 5b). These alkali feldspar granites have high

AC

Fe* [FeOT /(FeOT+ MgO)] values ranging from 0.89 to 0.91, and they plot in the ferroan field in a Fe* versus SiO2 diagram (Fig. 5c; Frost et al., 2001). They have low CaO contents (0.29–0.38 wt.%) and follow the alkali trend in a (K2O + Na2O – CaO) versus SiO2 diagram (Fig. 5d; Frost et al., 2001). These alkali feldspar granites have fractionated rare earth element (REE) patterns with (La/Yb)N of 5.51–7.88, high total REE abundances (ΣREE = 139.9–145.3 ppm), and distinct negative Eu anomalies (Eu/Eu* = 0.21–0.30; Fig. 6a; Boynton, 1984). They are also enriched in large ion lithophile elements (LILE; e.g., Rb and K), Pb, Th, and U, and depleted in Ba, P, and

ACCEPTED MANUSCRIPT Ti (Fig. 6b). In addition, these rocks have high Nb, Zr, Y, and Ce concentrations and high Ga/Al (2.57–2.65), similar to A-type granites (Whalen et al., 1987). 4.2.2 Carboniferous igneous rocks The Carboniferous igneous rocks consist of basaltic andesite, andesite, dacite, rhyolite, quartz monzodiorite, and monzogranite. These rocks have a varied major

PT

element composition (Figs. 5a and 7). Their Mg# [molar 100*Mg/(Mg + Fe)] range

RI

from 49 for the basaltic andesite to 5 for the rhyolite. The basaltic andesite and

SC

andesite are classified in the alkaline series in the TAS and (K2O + Na2O – CaO) versus SiO2 diagrams, whereas the other Carboniferous igneous rocks are classified as

NU

alkali-calcic or calc-alkalic (Fig. 5a). Their A/CNK values range from 0.83 to 1.16, indicative of metaluminous to weakly peraluminous compositions (Fig. 5b). In the

MA

Fe* versus SiO2 diagram, the quartz monzodiorite, basaltic andesite, andesite, and dacite plot in the magnesian field, whereas the monzogranite and rhyolite plot in the

D

ferroan field. The Carboniferous igneous rocks have ΣREE of 53.9–187.5 ppm and

PT E

varied Eu/Eu* of 0.36–1.00. The variation in trace element characteristics is related to sampling sites. Compared with the other Carboniferous igneous rocks (ΣREE =

CE

98.3–187.5 ppm), samples from the Yuejin Pluton display lower REE abundances (53.9–57.3 ppm). The REE patterns of all Carboniferous igneous rocks are

AC

characterized by enrichment in light rare earth elements (LREE) [(La/Yb)N = 5.26–17.15] and depletion in heavy rare earth elements (HREE; Fig. 6c). In a primitive-mantle-normalized trace element diagram (Fig. 6d), the samples show pronounced enrichment in LILE (e.g., Rb and K), Pb, Th, and U, and depletion in high field strength elements (HFSE; e.g., Nb, Ta and Ti). 4.3 In situ zircon Hf isotopic compositions The results of in situ Hf isotopic analysis of zircons from seven samples are

ACCEPTED MANUSCRIPT shown in Fig. 8. 4.3.1 Late Devonian intrusive rocks Eleven of 20 dated zircons from sample 15XH2-1 were chosen for in situ Hf isotopic analysis.

176

Hf/177Hf values vary from 0.282830 to 0.282908, yielding εHf(t)

values of +9.6 to +13.0 and two-stage model ages (TDM2) of 539–705 Ma.

PT

4.3.2 Carboniferous igneous rocks

RI

Fifty–seven dated zircons from Carboniferous igneous samples were chosen for

have

176

SC

in situ Hf isotopic analysis. Zircon grains from the Yuejin monzogranite (15XH2-1) Hf/177Hf values of 0.282725–0.282799, yielding εHf(t) values of +4.2 to +6.9

Zhangguangcailing

Complex

NU

and TDM2 ages of 814–965 Ma. Zircon grains from a rhyolite sample from the (HDY3-1)

yield

176

Hf/177Hf

values

of

MA

0.282889–0.282983, yielding εHf(t) values of +10.5 to +13.7, and TDM2 ages of 454–660 Ma. Zircon grains from the Wulidicun quartz monzodiorites (15XH19-1 and

D

16XH1-1) and volcanic rocks of the Heilonggong Formation (15XH18-1 and

PT E

16XH4-1) have similar Hf isotopic composition. Their176Hf/177Hf values vary from 0.282700 to 0.282892, yielding εHf(t) values of +5.8 to +10.7 and single-stage model

CE

(TDM1) ages of 532–757 Ma.

AC

5. Discussion

5.1 Petrogenesis of Late Devonian alkali feldspar granites The Devonian alkali feldspar granites have A/CNK values of 1.00–1.02, high Fe* and Ga/Al, and pronounced negative Eu anomalies, suggesting an affinity to A-type (Whalen et al., 1987; Chappell and White, 1992) or ferroan granites (Frost and Frost, 2011). Three main petrogenetic models have been proposed for the formation of A-type

ACCEPTED MANUSCRIPT granites: (1) extreme differentiation of mantle-derived basaltic magma (Eby, 1992; Vander Auwera, 2003; Frost and Frost, 2011; Papoutsa et al., 2016); (2) partial melting of granodioritic or tonalitic crust (Creaser et al., 1991; PatiñoDouce, 1997); and (3) partial melting of newly accreted mafic lower crust (Wu et al., 2002; Litvinovsky et al., 2015). Field observations did not reveal coeval mafic and

PT

intermediate igneous rocks, thereby excluding the possibility that the A-type granites

RI

formed via extreme differentiation of a mafic magma. Furthermore, the A-type

SC

granites contain high SiO2 and Al2O3 concentrations, have low Mg#, and extremely low Cr, Co, and Ni concentrations, further reducing the likelihood that they formed by

NU

extreme differentiation of mafic magma. In addition, previous experimental studies have suggested that dehydration melting of tonalitic or granodioritic crust takes place

MA

only in the shallow crust (Skjerlier and Johnston, 1993; PatiñoDouce, 1997), and cannot therefore explain the radiogenic Hf isotopic compositions of the studied

D

granites. Thus, we preclude the possibility that these A-type granites are formed by

PT E

partial melting of granodioritic or tonalitic crust (Creaser et al., 1991; PatiñoDouce, 1997). Taking this evidence into account, we conclude that the primary magmas for

CE

the A-type of granites were instead generated by partial melting of newly accreted mafic lower crust (Wu et al., 2002; Litvinovsky et al., 2015), which is also indicated

AC

by their high Th/Ta and Y/Nb, and low Ce/Pb values (Moreno et al., 2014). Based on the above observations, combined with the zircon εHf(t) values (+9.6 to +13.0) of the granites as well as their TDM2 ages of 539 to 705 Ma, we conclude that the Late Devonian alkali feldspar granites formed by partial melting of a late Neoproterozoic mafic lower crustal source. 5.2 Petrogenesis of Carboniferous intermediate–felsic igneous rocks 5.2.1 Petrogenetic relationships amongst the Carboniferous intermediate–felsic

ACCEPTED MANUSCRIPT igneous rocks The Carboniferous igneous rocks at the eastern margin of the SRM consist of a suite of intermediate–felsic igneous rocks (Fig. 5a). Here, we consider the petrological evolution of this suite and examine whether they have a genetic relationship or independent origins.

PT

Fifteen samples from the Wulidicun Pluton and the adjacent Heilonggong

RI

Formation are composed of quartz monzodiorite, basaltic andesite, andesite, dacite,

SC

and rhyolite. The crystallization ages of these rocks (325–315 Ma) are within error of each other and the rocks show consistent magmatic zircon Hf isotopic compositions

NU

(Fig. 8; εHf = +6.5 to +10.7), suggesting a genetic relationship. The large variation in SiO2 contents in these rocks is well correlated with variations in TiO2, Al2O3, Fe2O3,

MA

MgO, CaO, and K2O, as well as trace elements such as Zn and Sr (Fig. 7). Such linear compositional variations can be attributed to either fractional crystallization or mixing

D

between two end-member melts (e.g., mafic and felsic; Özdemir et al., 2011). Zr and

PT E

P have been recently applied in the modeling of fractional crystallization and magma mixing processes (Lee and Bachmann, 2014). These two elements are generally

CE

under–saturated in basaltic magmas and are progressively enriched in the evolving magma until the saturation point of zircon and apatite is reached, at which stage Zr

AC

and P are removed from the melt. Accordingly, the kink-shaped patterns in the SiO2 versus Zr and P2O5 diagrams (Fig. 7g and 7h) indicate that fractional crystallization, rather than magma mixing, was the major control on the formation of these rocks (Lee and Bachmann, 2014). This conclusion is further supported by the absence of mafic enclaves in the quartz monzodiorites. Fractionation of clinopyroxene and hornblende results in decrease of CaO, MgO, Fe2O3, and Dy/Yb with increasing SiO2 contents (Davidson et al., 2007). Decrease in Eu/Eu* and Sr concentrations with increasing

ACCEPTED MANUSCRIPT SiO2 can be related to the fractionation of plagioclase (Nandedkar et al., 2014), and variations in P2O5 and TiO2 likely reflect the removal of accessory minerals such as apatite and Fe–Ti oxides. The Yuejin monzogranites of the northern Zhangguangcai Range have significantly lower REE contents and zircon εHf values (+4.2 to +6.9) than coeval

PT

igneous rocks from the Wulidicun Pluton and Heilonggong Formation in the southern

RI

Zhangguangcai Range, indicating that the Yuejin monzogranites were derived from a

SC

different magma source. In addition, compared with rhyolites from the Heilonggong Formation, those from the Zhangguangcailing Complex have more evolved major and

NU

trace elemental compositions (Fig. 7), and lower Dy/Yb and Eu/Eu* values (Supplementary Table 2). It is possible that the rhyolites from the Zhangguangcailing

MA

Complex shared a common magma source with those from the Heilonggong Formation, but underwent a higher degree of fractional crystallization. Nevertheless,

D

considering that rhyolites from the Zhangguangcailing Complex have higher zircon

PT E

εHf values (+10.5 to +13.7) than rhyolitic rocks from the Heilonggong Formation, we conclude that they were derived from different magma sources.

CE

In conclusion, the Carboniferous igneous rocks of the Wulidicun Pluton and Heilonggong Formation have a genetic relationship, and the geochemical variations

coeval

AC

among these igneous rocks are attributed mainly to fractional crystallization, whereas monzogranites

from

the

Yuejin

Pluton

and

rhyolites

from

the

Zhangguangcailing Complex had independent origins. 5.2.2 Magma source As discussed above, the studied Carboniferous igneous rocks from the Wulidicun Pluton and the Heilonggong Formation formed by fractional crystallization; thus, the key question concerning their magmatic evolution is the composition of the primary

ACCEPTED MANUSCRIPT magma. However, it remains unclear whether the basaltic andesite (the most mafic rock examined in this study) represents the primary magma or is a product of differentiation from an initially more mafic primary magma. Thus, understanding the generation of the basaltic andesite is crucial in deducing the composition of the primary magma. Several hypotheses have been proposed for the generation of

PT

andesitic magma, including: (1) dehydration partial melting of meta-basaltic crust

RI

(e.g., Smith and Leeman, 1987; Petford and Atherton, 1996); (2) direct melting of the

SC

mantle under water–saturated conditions (e.g., Carmichael, 2002; Parman and Grove, 2004; Ashwal et al., 2016); (3) crystal fractionation of mantle-derived basalts in

NU

crustal magma chambers (e.g., Mortazavi and Sparks, 2004; Annen et al., 2006; Deering et al., 2011; Lee and Bachmann, 2014); and (4) mixing of mafic magmas

MA

with high-Si magmas (e.g., dacite–rhyolite) or crustal material (e.g., Rebui and Blundy, 2009). The analyzed basaltic andesite has a low SiO2 content (50.55 wt.%)

D

high concentrations of Sr (632 ppm), Cr (39.3 ppm), Co (27.9 ppm), and Ni (30.4

PT E

ppm), and a high Mg# (49), but lacks a Eu anomaly (Eu/Eu* = 1.00), which is inconsistent with a primary magma derived from partial melting of crustal rocks

CE

(Rapp et al., 1991; Rapp and Watson, 1995; Patiño Douce, 1999). Instead, we propose a mantle source. Furthermore, melting of the mantle generates magmas with low Zr

AC

(<50 ppm) and P2O5 (<0.2 wt.%; Workman and Hart, 2005), and high MgO concentrations (≥6.0 wt.%; Grove et al., 2003). However, the studied basaltic andesite has relatively high Zr (155 ppm) and P2O5 (0.36 wt.%) concentrations, and low MgO contents (4.60 wt.%), thereby precluding the possibility of an origin involving direct melting of the mantle. Moreover, its Cr, Co, and Ni contents are lower than those of a mantle-derived primary magma (Frey and Prinz, 1978), suggesting derivation from a relatively evolved basaltic melt. The production of an andesitic magma through

ACCEPTED MANUSCRIPT mixing fails to explain the kink-shaped patterns in the SiO2 versus Zr and P2O5 diagrams, because mixing processes produce linear arrays (Lee and Bachmann, 2014; Fig. 7g and 7h). For these reasons, we suggest that the basaltic andesite does not represent the primary magma, but was derived from crystal fractionation of a mantle–derived basaltic magma. Given that the basaltic andesite retains the most

PT

information on the composition of the primary magma, its geochemistry still reflects

RI

the nature of its mantle source. The basaltic andesite is enriched in LILE and depleted in HFSE, being geochemically similar to igneous rocks formed in subduction zones

SC

(Gill, 1981; McCulloch and Gamble, 1991). Considering the basaltic andesite’s zircon

NU

εHf values (+5.8 to +10.7), we conclude that the primary magma of the basaltic andesite and cogenetic igneous rocks was derived from partial melting of depleted

MA

mantle, previously metasomatized by subduction-related fluids. Rhyolites from the Zhangguangcailing Complex and monzogranites from the

D

Yuejin Pluton have relatively high SiO2 concentrations, low Mg#, and extremely low

PT E

contents of Cr, Co, and Ni, indicative of derivation from crustal sources. The rhyolites have zircon εHf(t) values of +10.5 to +13.7 and corresponding Hf TDM2 ages of

CE

454–660 Ma, suggesting that their primary magma was derived from partial melting of juvenile (early Paleozoic to late Neoproterozoic) lower continental crust.

AC

Compared with the rhyolites, the monzogranites have lower zircon εHf(t) values (+4.2 to +6.9) and relatively old Hf TDM2 ages (814–965 Ma), suggesting that their primary magma was derived from partial melting of slightly older crust. 5.3 Late Paleozoic tectonic evolution of the SRM The tectonic evolution of the SRM remains controversial because the timing of the amalgamation of the SRM and JM has been assigned to both the early Paleozoic (Li et al., 1999; Meng et al., 2010; Wang et al., 2012a, 2016, 2017) and the Jurassic

ACCEPTED MANUSCRIPT (Wu et al., 2007; Zhou et al., 2009; Zhu et al., 2015, 2017). Consequently, it remains unclear whether the late Paleozoic igneous rocks within the SRM formed during westward subduction beneath the SRM (Dong et al., 2017) or in a post-collisional setting, following the amalgamation of the two massifs (Xu et al., 2012). The Late Devonian–Carboniferous igneous rocks examined in this study, combined with

RI

important constraints on the tectonic evolution of the SRM.

PT

available literature data (Meng et al., 2010; Wang et al., 2012a), provide several

SC

The Late Devonian igneous rocks consist of alkali feldspar granites with an affinity to A-type granites, indicative of formation in an extensional setting

NU

(Dall’Agnol et al., 2012), rather than generation during subduction of an oceanic plate. This hypothesis is supported by the following points. (1) The amalgamation between

MA

the SRM and JM was probably completed by the early Devonian (Fig. 9a; Meng et al., 2010; Wang et al., 2012a). Firstly, the SN-trending subduction-related granitoids,

D

including diorites, tonalites and granodiotites with ages of ~485–450 Ma, are

PT E

documented in the eastern SRM (Wang et al., 2016), while the collision-related peraluminous monzogranites with ages of ~425 Ma are identified in the northern part

CE

of the studied area, implying that the amalgamation between the northern part of the SRM and JM had finished at the Middle Silurian (~425 Ma; Wang et al., 2012a).

AC

Secondly, the Early Devonian strata occurred in both the SRM and JM are unconformably overlying on the crystalline basement (Wang et al., 2008). Detrital zircons from sandstones of the Early Devonian strata in the eastern SRM yield U-Pb peak age populations of ~2500, ~1800, ~900–800, ~550 and 490–403 Ma, while detrital zircons from quartz sandstones of the Devonian Heitai Formation in the JM yield peak age populations of 569–542, ~509 and ~484 Ma. The abundant ~550 Ma ages obtained from both the SRM and JM are consistent with those from the

ACCEPTED MANUSCRIPT Pan-African metamorphosed Mashan Complex in the JM, implying that the JM had been a provenance for the Early Devonian sediments in the SRM. Taken together, we conclude that the amalgamation between the SRM and JM had completed prior to the Early Devonian (Meng et al., 2010). (2) The formation of ~390 Ma bimodal volcanic rocks in the JM, and A-type rhyolites in the eastern SRM, record the transition from a

PT

collisional to a post-collisional extensional environment (Meng et al., 2011).

RI

Moreover, the A-type rhyolites have extremely high zircon saturation temperatures

SC

(TZr = 903–939 °C). Such high-temperature A-type rhyolites most likely originated from the upwelling of hot asthenospheric material and subsequent partial melting of

and

von

Blanckenburg,

1995).

(3)

NU

the overlying crust following delamination of the lithospheric mantle (Huw Davies Devonian–early Carboniferous

marine

MA

sedimentary–volcanic formations, including quartz sandstone and carbonate rocks, occur within the southern SRM and JM, and were deposited in a passive continental

D

margin environment (JBGMR, 1988; Zhang et al., 2015), consistent with a

PT E

post-collisional extensional setting. Therefore, we suggest the Late Devonian A-type granites were generated during protracted post-collisional extension, related to

CE

collision of the SRM and JM (Fig. 9b). The Carboniferous igneous rocks consist of basaltic andesite, andesite, dacite,

AC

rhyolite, quartz monzodiorite and monzogranite. The basaltic andesite has a high Zr concentration (155 ppm) and high Zr/Y value (5.6), similar to within-plate basalts (Pearce and Norry, 1979). The Yuejin monzogranites, occurred in northern part of the studied area, exhibit steeper HREE patterns, probably suggesting the residue of garnet in the source, different from other Carboniferous granitoids occurred in southern part of the studied area. Previous studies have indicated that a collision between northern part of the SRM and the JM happened during late stage of early Paleozoic, whereas

ACCEPTED MANUSCRIPT this collision did not happen in its southern part (Wang et al., 2012a, 2016, 2017). Thus, we consider that the difference of nature of magma sources in northern part and its southern part of the studied area could be responsible for geochemical variations of Carboniferous granitoids. That is, the Yuejin monzogranites could be derived from partial melting of the previously thickened crustal material. Combined with the

PT

geochemical features of the Yuejin monzogranites such as significantly low LREE

RI

and Sr contents as well as obviously negative Eu anomalies (0.60-0.66), we conclude

SC

the Yuejin monzogranites formed in an extensional environment (Anderson, 1983; Forst and Forst, 2011). Hence, we suggest that the Carboniferous intermediate–felsic

NU

igneous rocks formed in a within-plate extensional setting (Fig. 9c). This conclusion is also supported by the following observations. (1) Late Carboniferous marine

MA

sediments (including thick mudstone and carbonate) occur along the southern margin of the SRM and JM, and were deposited in a passive continental margin setting

D

(Wang et al., 2008; Liu et al., 2017), whereas the coeval continental rifted trough

PT E

sediments (including terrestrial sandy conglomerate, sandstone, and siltstone) were deposited in the centre of these two massifs (Zhao et al., 1996; Liu et al., 2017). (2)

CE

Early Carboniferous (~340 Ma) alkaline granites at the southeastern margin of the SRM exhibit geochemical features typical of A-type granites (Wang et al., 2015), and

AC

are interpreted to form in a within-plate setting (Pearce, 1996). Therefore, we propose that the Carboniferous intermediate–felsic igneous rocks formed in a within-plate extensional tectonic setting. Subsequent extension may have persisted to the Permian, after which the JM was separated from the SRM (Meng et al., 2010; Xu et al., 2012; Yu et al., 2013). 5.4 Crustal growth and reworking within the SRM Zircon Hf isotopic data are particularly useful in tracking the processes of crustal

ACCEPTED MANUSCRIPT growth and reworking (e.g., Kemp et al., 2006; Belousova et al., 2010; Kröner et al., 2014; Vervoort and Kemp, 2016). However, the role of tectonic evolution in crustal processes has rarely been investigated using isotopic data (Kemp et al., 2009). The Paleozoic igneous rocks within the eastern SRM record a transition from subduction–collision to post-collision tectonics (Meng et al., 2011; Wang et al., 2012a,

PT

2016). Therefore, the zircon Hf isotopic data of the Paleozoic igneous rocks not only

RI

provide key insights into the crustal growth and reworking processes recorded in the

SC

eastern SRM, but yield a better understanding of the geodynamic controls on crustal evolution.

NU

The zircon Hf isotopic compositions of the studied late Paleozoic felsic igneous rocks show that crustal accretion in the eastern SRM occurred during the

MA

Neoproterozoic–early Paleozoic (TDM2 ages of 965–454 Ma). The Late Devonian alkali feldspar granites from the Yanshou Pluton and Carboniferous rhyolites from the

D

Zhangguangcailing Complex were derived from reworking of short-lived juvenile

PT E

(late Neoproterozoic to early Paleozoic) continental crust, whereas the Carboniferous monzogranites from the Yuejin Pluton are the products of the reworking of early

CE

Neoproterozoic crust.

When plotted as a function of crystallization age, zircon εHf data of Paleozoic

AC

igneous rocks from the eastern SRM define a striking temporal trend that correlates with tectonic evolution (Fig. 8). The early Paleozoic igneous rocks formed above a west-dipping subduction zone (Wang et al., 2012a, 2016), and their zircon Hf isotopic compositions are subdivided into two groups. Group 1 has εHf values ranging from –1 to +7.0 and TDM2 ages of 1.2–1.5 Ga, which are significantly older than their crystallization ages. This suggests that crustal growth in the eastern SRM occurred mainly in the Mesoproterozoic, and reworking of such crust occurred during the early

ACCEPTED MANUSCRIPT Paleozoic. Group 2 has lower εHf values (–8.6 to –3.7) and older TDM2 ages (1.7–2.0 Ga), thereby supporting the existence of Paleoproterozoic basement material as proposed by Pei et al. (2007) and Meng et al. (2010). These variations in zircon Hf isotopic compositions also provide evidence for the heterogeneity of the deep crust in the study area. The late Paleozoic magmatism marked the switch from a

PT

subduction–collision to post-collisional extensional setting. Implicit within this

RI

tectonic transition scenario are changes in magma source, mirrored by an increase in

SC

εHf values. The zircon Hf isotopic signatures of the 360–390 Ma igneous rocks are controlled by reworking of short-lived juvenile continental crust. The zircon Hf

NU

isotopic compositions and whole-rock geochemical characteristics of the ~320 Ma igneous rocks record the input of a mantle-derived basaltic magma and interaction

MA

with the surrounding short-lived juvenile or slightly older crust. Zircon εHf(t) values become less radiogenic from 390 to 250 Ma, implying that older crustal materials

D

became involved in the generation of the late Paleozoic igneous rocks. Enhanced

PT E

older crustal input could have occurred due to reworking of pre-existing Mesoproterozoic crust or contamination during magma ascent through the upper crust.

CE

In conclusion, we have shown that the early Paleozoic granitoids were derived from the reworking of heterogeneous ancient crust, and that reworking of short-lived

AC

juvenile continental crust occurred in the early late Paleozoic in a post-collisional extensional setting.

6. Conclusions Based on the zircon U–Pb ages, Hf isotopic data, and geochemical data presented above, we draw the following conclusions. 1. Two late Paleozoic magmatic events are recorded within the eastern SRM: Late Devonian (366 Ma) and Carboniferous (325–313 Ma).

ACCEPTED MANUSCRIPT 2. The Late Devonian magmatic event produced alkali feldspar granites with an affinity to A-type granite. The Late Devonian granitic magma was derived from partial melting of Neoproterozoic lower crust and formed in a post-collisional extensional environment. 3. The Carboniferous magmatic event produced a suite of intermediate–felsic

PT

igneous rocks. Basaltic andesite, andesite, dacite, and rhyolite from the Heilonggong

RI

Formation and Wulidicun quartz monzodiorites formed by fractional crystallization

SC

from a basaltic magma that was produced during partial melting of a hydrated depleted mantle. Monzogranites from the Yuejin Pluton and rhyolites from the

NU

Zhangguagncailing Complex were generated by partial melting of separate juvenile crustal sources. Carboniferous magmatism occurred in a within-plate extensional

MA

setting.

4. Zircon Hf isotopic compositions of the Paleozoic felsic igneous rocks reveal

D

that crustal accretion beneath the SRM took place in the Mesoproterozoic and

PT E

Neoproterozoic (as well as minor early Paleozoic), and that reworking of short-lived

CE

juvenile continental crust occurred in the early late Paleozoic.

Acknowledgements

AC

We thank the staff of the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Wuhan, and the Geological Laboratory Centre, China University of Geosciences, Beijing, for their advice and assistance during zircon LA–ICP–MS U–Pb dating, major and trace element analyses, and zircon Hf isotope analysis. We also thank the journal associate editor Dr. K. Sajeev and two anonymous reviewers for their constructive comments and suggestions. This work was financially supported by the National Natural Science

ACCEPTED MANUSCRIPT Foundation of China (Grant41330206), National Key Research and Development Project (2017YFC0601304), and the Opening Foundation of the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences (Wuhan) (Grant GPMR201503).

PT

References

RI

Anderson, J. L., 1983. Proterozoic anorogenic granite plutonism of North America.

SC

Geological Society of America, Memoirs 161, 133-154.

Anderson, T., 2002. Correction of common lead in U-Pb analyses that do not report

NU

204Pb. Chemical Geology 192, 59–79.

Annen, C., Blundy, J.D., Sparks, R.S.J., 2006. The genesis of intermediate and silicic

MA

magmas in deep crustal hot zones. Journal of Petrology 47, 505–539. Ashwal, L., Torsvik, T., Horváth, P., Harris, C., Webb, S., Werner, S., Corfu, F., 2016.

PT E

1645-1675.

D

A mantle-derived origin for Mauritian trachytes. Journal of Petrology 57(9),

Atherton, M.P., Petford, N., 1993, Generation of sodium-rich magmas from newly

CE

underplated basaltic crust. Nature 362, 144–146. Belousova , E.A., Kostitsyn, Y.A., Griffin, W.L., Begg, G.C., O'Reilly, S.Y., Pearson,

AC

N.J., 2010. The growth of the continental crust: Constraints from zircon Hf-isotope data. Lithos 119, 457-466. Bi, J.H., Ge, W.C., Yang, H., Wang, Z.H., Dong, Y., Liu, X.W., Ji, Z., 2017. Age, petrogenesis, and tectonic setting of the Permian bimodal volcanic rocks in the eastern Jiamusi Massif, NE China. Journal of Asian Earth Sciences 134, 160–175. Bi, J.H., Ge, W.C., Yang, H., Zhao, G.C., Yu, J.J., Zhang, Y.L., Wang, Z.H., Tian,

ACCEPTED MANUSCRIPT D.X., 2014. Petrogenesis and tectonic implications of early Paleozoic granitic magmatism in the Jiamusi Massif, NE China: geochronological, geochemical and Hf isotopic evidence. Journal of Asian Earth Sciences 96 (15), 308–331. Blichert-Toft, J., Albarède, F., 1997. The Lu-Hf geochemistry of chondrites and the evolution of the mantle-crust system. Earth and Planetary Science Letters 148,

PT

243-258.

RI

Boynton, W.V., 1984. Geochemistry of the rare earth elements: meteorite studies. In:

SC

Henderson, P. (Ed.), Rare Earth Element Geochemistry. Elservier, pp. 63-114. Cao, H.H., Xu,W.L., Pei, F.P.,Wang, Z.W.,Wang, F.,Wang, Z.J., 2013. Zircon U–Pb

NU

geochronology and petrogenesis of the Late Paleozoic–Early Mesozoic intrusive

Lithos 170–171, 191–207.

MA

rocks in the eastern segment of the northern margin of the North China Block.

Cao, X., Dang, Z.X., Zhang, X.Z., Jiang, J.S., Wang, H.D., 1992. Jiamusi Composite

D

Terranes. Jilin Publishing House of Science and Technology, Changchun, pp.

PT E

121–224 (in Chinese with English and Russian abstracts). Carmichael, I.S.E. 2002. The andesite aqueduct: perspectives on the evolution of

CE

intermediate magmatism in west–central (105–99°W) Mexico. Contributions to Mineralogy and Petrology 143, 641–663.

AC

Chappell, B.W., White, A.J.R., 1992. I- and S-type granites in the Lachlan Fold Belt. Transactions of the Royal Society of Edinburgh. Earth Sciences 83, 1–26. Chen, B., Jahn, B.M., Tian, W., 2009. Evolution of the Solonker suture zone: Constraints from zircon U–Pb ages, Hf isotopic ratios and whole-rock Nd-Sr isotope compositions of subduction-and collision-related magmas and forearc sediments. Journal of Asian Earth Sciences 34, 245–257. Chen, B., Jahn, B.M., Wilde, S., Xu, B., 2000. Two contrasting Paleozoic magmatic

ACCEPTED MANUSCRIPT belts in northern Inner Mongolia, China: petrogenesis and tectonic implications. Tectonophysics 328, 157–182. Creaser, R.A., Price, R.C., Wormald, R.J., 1991. A-type granites revisited: assessment of a residual-source model. Geology 19, 163-166. Dall'Agnol, R., Frost, C.D., Rämö, O.T., (Guest Ass. Eds.), 2012. A-type granites and

PT

related rocks, Special Issue. Lithos 151, 1–16.

SC

“sponge” in arc crust?. Geology 35(9), 787-790.

RI

Davidson, J., Turner, S., Handley, H., MacPherson, C., Dosseto, A., 2007. Amphibole

Davies, J.H., Blanckenburg, F.V., 1995. Slab breakoff: a model of lithosphere

NU

detachment and its test in the magmatism and deformation of collisional orogens. Earth and Planetary Science Letters, 129(1–4), 85-102.

MA

Deering, C.D., Bachmann, O., Dufek, J., Gravley, D.M., 2011. Rift-related transition from andesite to rhyolite volcanism in the Taupo volcanic zone (New Zealand)

D

controlled by crystal-melt dynamics in mush zones with variable mineral

PT E

assemblages. Journal of Petrology 52, 2243–2263. Dong, Y., Ge, W.C., Yang, H., Xu, W.L., Bi, J.H., Wang, Z.H., 2017. Geochemistry

CE

and geochronology of the Late Permian mafic intrusions along the boundary area of Jiamusi and Songnen-Zhangguangcai Range massifs and adjacent regions,

AC

northeastern China: petrogenesis and implications for the tectonic evolution of the Mudanjiang Ocean. Tectonophysics 694, 356-367. Eby, G.N., 1992. Chemical subdivision of A-type granitoids: petrogenetic and tectonic implications. Geology 20, 641–644. Frey, F.A., Prinz, M., 1978. Ultramafic inclusions from San Carlos, Arizona: petrologic and geochemical data bearing on their petrogenesis. Earth and Planetary Science Letters 38, 129–176.

ACCEPTED MANUSCRIPT Frost, B.R., Arculus, R.J., Barnes, C.G., Collins, W.J., Ellis, D.J., Frost, C.D., 2001. A geochemical classification of granitic rocks. Journal of Petrology 42, 2033–2048. Frost, C.D., Frost, B.R., 2011. On ferroan (A-type) granitoids: their compositional variability and modes of origin. Journal of Petrology 52, 39–55.

PT

Gao, F.H., Xu, W.L., Yang, D.B., Pei, F.P., Liu, X.M., Hu, Z.C., 2007. LA-ICP-MS

RI

zircon U–Pb dating from granitoids in southern basement of Songliao basin:

SC

constraints on ages of the basin basement. Science in China Series D: Earth Sciences 50, 995–1004.

NU

Ge, M.H., Zhang, J.J., Liu, K., Ling, Y.Y., Wang, M.,Wang, J.M., 2016. Geochemistry and geochronology of the blueschist in the Heilongjiang Complex

MA

and its implications in the late Paleozoic tectonics of eastern NE China. Lithos 261, 232-249.

PT E

385–389.

D

Gill, J.B., 1981. Orogenic andesites and plate tectonics. New York, Springer, p.

Griffin, W.L., Wang, X., Jackson, S.E., Pearson, N.J., O’Reilly, S.Y., Xu, X.S., Zhou,

CE

X.M., 2002. Zircon chemistry and magma mixing, SE China: In-situ analysis of Hf isotopes, Tonglu and Pingtan igneous complexes. Lithos 61, 237–269.

AC

Grove, T.L., Elkins-Tanton, L.T., Parman, S.W., Chatterjee, N., Müntener, O., Gaetani, G.A., 2003. Fractional crystallization and mantle-melting controls on calc-alkaline differentiation trends. Contributions to Mineralogy and Petrology 145(5), 515-533. HBGMR (Heilongjiang Bureau of Geology and Mineral Resources), 1993. Regional Geology of Heilongjiang Province. Geological Publishing House, Beijing, pp. 1-418 (in Chinese with English abstract).

ACCEPTED MANUSCRIPT Hu, Z.C., Liu, Y.S., Gao, S., Liu, W.G., Yang, L., Zhang, W., Tong, X.R., Lin, L., Zong, K.Q., Li, M., Chen, H.H., Zhou, L., 2012. Improved in situ Hf isotope ratio analysis of zircon using newly designed X skimmer cone and jet sample cone in combination with the addition of nitrogen by laser ablation multiple collector ICP-MS. Journal of Analytical Atomic Spectrometry 27, 1391–1399.

PT

Irvine, T.H., Baragar, W.R.A., 1971. A guide to the chemical classification of the

RI

common volcanic rocks. Canadian Journal of Earth Sciences 8, 523–548.

SC

Jahn, B.M., 2004. The Central Asian Orogenic Belt and growth of the continental crust in the Phanerozoic. In: Malpas, J., Fletcher, C.J.N., Ali, J.R., Aitchison, J.C.

Special Publication 226, pp. 73–100.

NU

(Eds.), Aspects of the Tectonic Evolution of China. Geological Society London

MA

Jahn, B.M., Wu, F.Y., Chen, B., 2000. Massive granitoid generation in central Asia: Nd isotopic evidence and implication for continental growth in the Phanerozoic.

D

Episodes 23, 82–92.

PT E

JBGMR (Jilin Bureau of Geology and Mineral Resources), 1988. Regional Geology of Jilin Province. Geological Publishing House, Beijing, pp. 1–698 (in Chinese

CE

with English summary).

Jian, P., Liu, D.Y., Kröner, A., Windley, B.F., Shi, Y.R., Zhang, W., Zhang, F.Q.,

AC

Miao, L.C., Zhang, L.Q., Tomurhuu, D., 2010. Evolution of a Permian intraoceanic arc-trench system in the Solonker suture zone, Central Asian Orogenic Belt, China and Mongolia. Lithos 118, 169–190. Kemp, A.I.S., Hawkesworth, C.J., Collins, W.J., Gray, C.M., Blevin, P.L., 2009. Isotopic evidence for rapid continental growth in an extensional accretionary orogen: The Tasmanides, eastern Australia. Earth and Planetary Science Letters 284, 455–466.

ACCEPTED MANUSCRIPT Kemp, A.I.S., Hawkesworth, C.J., Paterson, B.A., Kinny, P., 2006. Episodic growth of the Gondwana Supercontinent from hafnium and oxygen isotopes in zircon. Nature 439, 580–583. Koschek, G., 1993. Origin and significance of the SEM cathodoluminescence from zircon. Journal of Microscopy 171, 223–232.

PT

Kröner, A., Kovach, V., Belousova, E., Hegner, E., Armstrong, R., Dolgopolova, A.,

RI

Seltmann, R., Alexeiev, D.V., Hoffmann, J.E., Wong, J., Sun, M., Cai, K., Wang,

SC

T., Tong, Y., Wilde, S.A., Degtyarev, K.E., and Rytsk, E., 2014. Reassessment of continental growth during the accretionary history of the Central Asian

NU

Orogenic Belt: Gondwana Research 25, 103–125.

Lee, C.-T.A., Bachmann, O., 2014. How important is the role of crystal fractionation

MA

in making intermediate magmas? Insights from Zr and P systematics. Earth and Planetary Science Letters 393, 266-274.

D

Li, J.Y., 2006. Permian geodynamic setting of Northeast China and adjacent regions:

PT E

closure of the Paleo-Asian Ocean and subduction of the Paleo-Pacific plate. Journal of Asian Earth Sciences 26, 207–224.

CE

Li, J.Y., Niu, B.G., Song, B., Xu, W.X., Zhang, Y.H., Zhao, Z.R., 1999. Crustal Formation and Evolution of Northern Changbaishan Mountains, Northeast China.

AC

Geological Publishing House, Beijing (in Chinese). Li, S., Chung, S. L., Wilde, S. A., Wang, T., Xiao, W. J., Guo, Q. Q., 2016. Linking magmatism with collision in an accretionary orogen. Scientific Reports 6: 25751. Litvinovsky, B.A., Jahn, B.M., Eyal, M., 2015. Mantle-derived sources of syenites from the A-type igneous suites-New approach to the provenance of alkaline silicic magmas. Lithos 232, 242-265. Liu, Y.J., Li,W.M., Feng, Z.Q., Wen, Q.B., Neubauer, F., Liang, C.Y., 2017. A

ACCEPTED MANUSCRIPT review of the Paleozoic tectonics in the eastern part of Central Asian Orogenic Belt. Gondwana Research 43, 123–148. Liu, Y.S., Hu, Z.C., Zong, K.Q., Gao, C.G., Gao, S., Xu, J., Chen, H.H., 2010. Reappraisement and refinement of zircon U–Pb isotope and trace element analyses by LA-ICP-MS. Chinese Science Bulletin 55, 1535-1546.

PT

Liu, Y.S., Zong, K.Q., Kelemen, P.B., Gao, S., 2008. Geochemistry and magmatic

RI

history of eclogites and ultramafic rocks from the Chinese continental scientific

SC

drill hole: subduction and ultrahigh-pressure metamorphism of lower crustal cumulates. Chemical Geology 247 (1-2), 133–153.

NU

Luan, J.P., Xu,W.L., Wang, F.., Wang, Z.W., Guo, P., 2017. Age and geochemistry of the Neoproterozoic granitoids in the the Songnen-Zhangguangcai Range Massif,

MA

NE China: Petrogenesis and tectonic implications. Journal of Asian Earth Sciences 148, 265–276.

D

Ludwig, K.R., 2003. User's manual for ISOPLOT 3.00: a geochronological toolkit for

PT E

Microsoft excel. Berkeley Geochronology Center Special Publication 4, 1–70. McCulloch, M.T., Gamble, J.A., 1991. Geochemical and geodynamical constraints on

CE

subduction zone magmatism. Earth and Planetary Science Letters 102, 358–374. Meng, E., Xu, W.L., Pei, F.P., Wang, F., 2011c. Middle Devonian volcanism in

AC

eastern Heilongjiang Province and its tectonic implications: constraints from petrogeochemistry, zircon U–Pb chronology and Sr–Nd–Hf isotopes. Acta Petrologica et Mineralogica 30, 883–900 (in Chinese with English abstract). Meng, E., Xu, W.L., Pei, F.P., Yang, D.B., Yu, Y., Zhang, X.Z., 2010. Detrital-zircon geochronology of Late Paleozoic sedimentary rocks in eastern Heilongjiang Province, NE China: implications for the tectonic evolution of the eastern segment of the Central Asian Orogenic Belt. Tectonophysics 53, 1231–1245.

ACCEPTED MANUSCRIPT Moreno, J. A., Molina, J. F., Montero, P., Anbar, M. A., Scarrow, J. H., Cambeses, A., Bea, F., 2014. Unraveling sources of a-type magmas in juvenile continental crust: constraints from compositionally diverse ediacaran post-collisional granitoids in the katerina ring complex, southern sinai, Egypt. Lithos 192-195, 56-85. Mortazavi, M., Sparks, R.S.J., 2004. Origin of rhyolite and rhyodacite lavas and

PT

associated mafic inclusions of Cape Akrotiri, Santorini: the role of wet basalt in

RI

generating calcalkaline silicic magmas. Contributions to Mineralogy and

SC

Petrology 146, 397–413.

Nandedkar, R.H., Ulmer, P., Muentener, O., 2014. Fractional crystallization of

NU

primitive, hydrous arc magmas: an experimental study at 0.7 GPa. Contributions to Mineralogy and Petrology 167, 1015.

MA

Özdemir, Y., Blundy, J., Gulec, N., 2011. The importance of fractional crystallization and magma mixing in controlling chemical differentiation at Süphan

PT E

Petrology 162, 573–597.

D

stratovol-cano, eastern Anatolia, Turkey. Contributions to Mineralogy and

Papoutsa, A., Piper, G.P., Piper, D.J.W., 2016. Systematic mineralogical diversity in

CE

A-type granitic intrusions: control of magmatic source and geological processes. The Geological Society of America Bulletin, 128 (3–4), 487–501.

AC

Parman, S.W., Grove, T.L., 2004. Harzburgite melting with and without H2O: experimental data and predictive modeling. Journal of Geophysical Research 109(B02201), doi:10.1029/2003JB002566. Patiño Douce, A., 1997. Generation of metaluminous A-type granites by low-pressure melting of calc-alkaline granitoids. Geology 25, 743-746. Patiño Douce, A.E., 1999. What do experiments tell us about the relative contributions of crust and mantle to the origin of granitic magmas? Geological

ACCEPTED MANUSCRIPT Society Special Publications 168, 55–75. Pearce, J.A., 1996. Sources and settings of granitic rocks. Episodes 19 (4), 120–125. Pearce, J.A., Norry, M.J., 1979. Petrogenetic Implications of Ti, Zr, Y, and Nb Variations in Volcanic Rocks. Contributions to Mineralogy and Petrology 69, 33-47.

PT

Pei, F.P., Xu,W.L., Yang, D.B., Zhao, Q.G., Liu, X.M., Hu, Z.C., 2007. Zircon U–Pb

RI

geochronology of basement metamorphic rocks in the Songliao Basin. Chinese

SC

Science Bulletin 52 (7), 942–948.

Petford, N., Atherton, M., 1996. Na-rich partial melts from newly underplated basaltic

NU

crust: the Cordillera Blanca Batholith, Peru. Journal of Petrology 37, 1491–1521. Pupin, J.P., 1980. Zircon and granite petrology. Contributions to Mineralogy and

MA

Petrology 73, 207–220.

Rapp, R. P., Watson, E. B., 1995. Dehydration melting of metabasalt at 8–32

PT E

Petrology 36, 891–931.

D

kbar—implications for continental growth and crust–mantle recycling. Journal of

Rapp, R. P., Watson, E. B., Miller, C. F., 1991. Partial melting of amphibolite/eclogite

1-25.

CE

and the origin of Archean trondhjemites and tonalites. Precambrian Research 51,

AC

Reubi, O., Blundy, J., 2009. A dearth of intermediate melts at subduction zone volcanoes and the petrogenesis of arc andesites. Nature 461, 1269–1274. Rudnick, R.L., Gao, S., Ling, W.L., Liu, Y.S., McDonough, W.F., 2004. Petrology and geochemistry of spinel peridotite xenoliths from Hannuoba and Qixia, North China Craton. Lithos 77, 609–637. Safonova, I.Y., Santosh, M., 2014. Accretionary complexes in the Asia-Pacific region: tracing archives of ocean plate stratigraphy and tracking mantle plumes.

ACCEPTED MANUSCRIPT Gondwana Research 25, 126–158. Sengör, A.M.C., Natal'in, B.A., Burtman, V.S., 1993. Evolution of the Altaid tectonic collage and Paleozoic crustal growth in Eurasia. Nature 364, 299–307. Skjerlie, K.P., Johnston, A.D., 1993. Fluid-absent melting behavior of an F-rich

anorogenic granites. Journal of Petrology 34, 785–815.

PT

tonalitic gneiss at mid-crustal pressures: implications for the generation of

RI

Smith, D.R. Leeman, W.P., 1987. Petrogenesis of Mount St. Helens dacitic magmas.

SC

Journal of Geophysical Research 92, 10313–10334.

Sun, S.S., McDonough, W.F., 1989. Chemical and isotopic systematics of oceanic

NU

basalts: implications for mantle composition and processes. In: Saunders, A.D., Norry, M.J. (Eds.), Magmatism in Ocean Basins. Geological Society of Special

MA

Publications, London, pp. 313–345.

Vander Auwera, J., 2003. Preface. Origin and evolution of Precambrian anorogenic

D

magmatism. Precambrian Research 124, 105–106.

PT E

Vervoort, J.D., Kemp, A.I.S., 2016. Clarifying the zircon Hf isotope record of crust-mantle evolution. Chemical Geology 425, 65–75.

CE

Wang, C.W., Jin,W., Zhang, X.Z., Ma, Z.H., Chi, X.G., Liu, Y.J., Li, N., 2008. New understanding of the late paleozoic tectonics in northeastern china and adjacent

AC

areas. Journal of Stratigraphy 32, 119–136 (in Chinese with English abstract). Wang, F., Xu, W.L., Gao, F.H., Meng, E., Cao, H.H., Zhao, L., Yang, Y., 2012b. Tectonic history of the Zhangguangcailing Group in eastern Heilongjiang Province, NE China: constraints from U–Pb geochronology of detrital zircons. Tectonophysics 566-567, 105-122. Wang, F., Xu, W.L., Gao, F.H., Zhang, H.H., Pei, F.P., Zhao, L., Yang, Y., 2014. Precambrian terrane within the Songnen-Zhangguangcai Range Massif, NE

ACCEPTED MANUSCRIPT China: evidence from U-Pb ages of detrital zircons from the Dongfengshan and Tadong groups. Gondwana Research 26, 402–413. Wang, F., Xu, W.L., Meng, E., Cao, H.H., Gao, F.H., 2012a. Early Paleozoic amalgamation of the Songnen–Zhangguangcai Range and Jiamusi massifs in the eastern segment of the Central Asian Orogenic Belt: Geochronological and

PT

geochemical evidence from granitoids and rhyolites. Journal of Asian Earth

RI

Sciences 49, 234–248.

SC

Wang, F., Zhang, F.Q., Zhang, D.W., Miao, L.C., Li, T.S., Xie, H.Q., Meng, Q.R., Li, D.Y., 2006. Zircon SHRIMP U-Pb dating of meta-diorite from the basement of

NU

the Songliao Basin and its geological significance. Chinese Science Bulletin 51 (15), 1877-1883.

MA

Wang, Z.W., Pei, F.P., Xu, W.L., Cao, H.H., Wang, Z.J., 2015. Geochronology and geochemistry of Late Devonian and early Carboniferous igneous rocks of central

D

Jilin Province, NE China: Implications for the tectonic evolution of the eastern

PT E

Central Asian Orogenic Belt. Journal of Asian Earth Sciences 97, 260–278. Wang, Z.W., Xu, W.L., Pei, F.P., Wang, F., Guo, P., 2016. Geochronology and

CE

geochemistry of early Paleozoic igneous rocks of the Lesser Xing'an Range, NE China: Implications for the tectonic evolution of the eastern Central Asian

AC

Orogenic Belt. Lithos 261, 144–163. Wang, Z.W., Xu, W.L., Pei, F.P., Wang, F., Guo, P., Wang, F., Li, Y., 2017. Geochronology and geochemistry of early Paleozoic igneous rocks from the Zhangguangcai Range, northeastern China: Constraints on tectonic evolution of the eastern Central Asian Orogenic Belt. Lithosphere 9(5), 803-827. Whalen, J.B., Currie, K.L., Chappell, B.W., 1987. A-type granites: geochemical characteristics, discrimination and petrogenesis. Contributions to Mineralogy and

ACCEPTED MANUSCRIPT Petrology 95, 407–419. Wilde, S.A., Dorsett-Bain, H.L., Liu, J.L., 1997. The identification of a Late Pan-African granulite facies event in northeastern China: SHRIMP U-Pb zircon dating of the Mashan Group at Liu Mao, Heilongjiang Province, China. Proceedings of the 30th IGC: Precambrian Geology and Metamorphic Petrology,

PT

VSP International 17. Science Publishers, Amsterdam, pp. 59–74.

RI

Wilde, S.A., Wu, F.Y., Zhang, X.Z., 2003. Late pan-African magmatism in

SC

northeastern China: SHRIMP U–Pb zircon evidence for igneous ages from the Mashan complex. Precambrian Research 122, 311-327.

NU

Wilde, S.A., Zhang, X.Z.,Wu, F.Y., 2000. Extension of a newly-identified 500Ma metamorphic terrain in northeast China: further U–Pb SHRIMP dating of the

MA

Mashan complex, Heilongjiang Province, China. Tectonophysics 328, 115-130. Windley, B.F., Alexeiev, D., Xiao, W.J., Kröner, A., Badarch, G., 2007. Tectonic

D

model for accretion of the Central Asian Orogenic Belt. Journal of Geological

PT E

Society, London 164, 31–47.

Workman, R.K., Hart, S.R., 2005. Major and trace element composition of the

53–72.

CE

depleted MORB mantle (DMM). Earth and Planetary Science Letters 231,

AC

Wu, F.Y., Jahn, B.M., Wilde, S., Sun, D.Y., 2000. Phanerozoic continental crustal growth: Sr–Nd isotopic evidence from the granites in northeastern China. Tectonophysics 328, 89–113. Wu, F.Y., Jahn, B.M.,Wilde, S.A., Lo, C.H., Yui, T.F., Lin, Q., Ge,W.C., Sun, D.Y., 2003. Highly fractionated I-type granites in NE China (II): isotopic geochemistry and implications for crustal growth in the Phanerozoic. Lithos 67, 191-204. Wu, F.Y., Sun, D.Y., Ge, W.C., Zhang, Y.B., Grant, M.L.,Wilde, S.A., Jahn, B.M.,

ACCEPTED MANUSCRIPT 2011. Geochronology of the Phanerozoic granitoids in northeastern China. Journal of Asian Earth Sciences 41, 1–30. Wu, F.Y., Sun, D.Y., Li, H.M., Jahn, B.M., Wilde, S.A., 2002. A-type granites in Northeastern China: age and geochemical constraints on their petrogenesis. Chemical Geology 187, 143-171.

PT

Wu, F.Y., Yang, J.H., Lo, C.H., Wilde, S.A., Sun, D.Y., Jahn, B.M., 2007. The

RI

Heilongjiang Group: a Jurassic accretionary complex in the Jiamusi Massif at the

SC

western Pacific margin of northeastern China. Island Arc 16 (1), 156–172. Xiao, W.J., Windley, B.F., Hao, J., Zhai., M.G., 2003. Accretion leading to collision

NU

and the Permian Solonker suture, Inner Mongolia, China: Termination of the Central Asian Orogenic Belt. Tectonics 22, 1069–1090.

MA

Xiao, W.J., Windley, B.F., Sun, S., Li, J.L., Huang, B.C., Han, C.M., Yuan, C., Sun, M., and Chen, H.L., 2015. A Tale of Amalgamation of Three Permo-Triassic

D

Collage Systems in Central Asia: Oroclines, Sutures, and Terminal Accretion:

PT E

Annual Review of Earth & Planetary Sciences 43, 477–507. Xu, B., Charvet, J., Chen, Y., Zhao, P., Shi, G.Z., 2013a. Middle Paleozoic

CE

convergent orogenic belts in western Inner Mongolia (China): framework, kinematics, geochronology and implications for tectonic evolution of the Central

AC

Asian Orogenic Belt. Gondwana Research 23, 1342–1364. Xu, B., Zhao, P., Wang, Y.Y., Liao, W., Luo, Z.W., Bao, Q.Z., Zhou, Y.H., 2015. The pre- Devonian tectonic framework of Xing'an-Mongolia orogenic belt (XMOB) in north China. Journal of Asian Earth Sciences 97, 183–196. Xu, W.L., Wang, F., Meng, E., Gao, F.H., Pei, F.P., Yu, J.J., Tang, J., 2012. Paleozoic-Early Mesozoic Tectonic Evolution in the Eastern Heilongjiang Province, NE China: evidence from Igneous Rock Association and U-Pb

ACCEPTED MANUSCRIPT Geochronology of Detrital Zircons. Journal of Jilin University (Earth Science Edition) 42 (5), 1378–1389 (in Chinese with English abstract). Xu, W.L., Pei, F.P.,Wang, F., Meng, E., Ji,W.Q., Yang, D.B.,Wang,W., 2013b. Spatial-temporal Relationships of Mesozoic Volcanic Rocks in NE China: constraints on Tectonic Overprinting and Transformations Between Multiple

PT

Tectonic Regimes. Journal of Asian Earth Sciences 74, 167-193.

RI

Yang, H., Ge, W.C., Zhao, G.C., Dong, Y., Bi, J.H., Wang, Z.H., Yu, J.J., Zhang,

SC

Y.L., 2014. Geochronology and geochemistry of Late Pan-African intrusive rocks in the Jiamusi-Khanka Block, NE China: petrogenesis and geodynamic

NU

implications. Lithos 208-209, 220-236.

Yang, H., Ge, W.C., Zhao, G.C., Bi, J.H., Wang, Z.H., Dong, Y., Yu, J.J., Xu, W.L.,

MA

2017. Zircon U–Pb ages and geochemistry of newly discovered Neoproterozoic orthogneisses in the Mishan region, NE China: Constraints on the high-grade

PT E

268-271, 16-31.

D

metamorphism and tectonic affinity of the Jiamusi–Khanka Block. Lithos

Yu, J.J., Wang, F., Xu, W.L., Gao, F.H., Tang, J., 2013. Late Permian tectonic

CE

evolution at the southeastern margin of the Songnen–Zhangguangcai Range Massif, NE China: Constraints from geochronology and geochemistry of

AC

granitoids. Gondwana Research 24, 635–647. Zhang, X.Z., Guo, Y., Zhou, J.B., Zeng, Z., Pu, J.B., Fu, Q.L., 2015. Late Paleozoic Early Mesozoic Tectonic Evolution in the East Margin of the Jiamusi Massif, Eastern Northeastern China. Russian Journal of Pacific Geology 9(1), 1-10. Zhao, C.J., Peng, Y.J., Dang, Z.X., Zhang, Y.P., 1996. Tectonic Framework and Crust Evolution of Eastern Jilin and Heilongjiang Provinces. Liaoning University Press, Shenyang, pp. 1–186 (in Chinese with English abstract).

ACCEPTED MANUSCRIPT Zhou, J.B., Wilde, S.A., Zhang, X.Z., Zhao, G.C., Zheng, C.Q., Wang, Y.J., Zhang, X.H., 2009. The onset of Pacific margin accretion in NE China: evidence from the Heilongjiang high-pressure metamorphic belt. Tectonophysics 478, 230–246. Zhu, C.Y., Zhao, G.C., Sun, M., Eizenhöfer, P.R., Liu, Q., Zhang, X.R., 2017. Geochronology and geochemistry of the Yilan greenschists and amphibolites in

PT

the Heilongjiang Complex, northeastern China and tectonic implications.

RI

Gondwana Research 43, 213-228.

SC

Zhu, C.Y., Zhao, G.C., Sun, M., Liu, Q., Han, Y.G., Hou, W., Zhang, X.R., Eizenhofer, P.R., 2015. Geochronology and geochemistry of the Yilan

MA

implications. Lithos 216, 241–253.

NU

blueschists in the Heilongjiang Complex, northeastern China and tectonic

Figure Captions

D

Figure 1. (a) Simplified regional map showing known extent of Central Asian

PT E

Orogenic Belt, modified after Safonova and Santosh (2014). (b) Distribution of Devonian–Carboniferous magmatic rocks within the eastern SRM and JM. ① suture;

② Dunhua–Mishan Fault;

③

CE

Solonker–XarMoron–Changchun–Yanji

AC

Yitong–Yilan Fault; ④ Jiayin–Mudanjiang Fault. (c) Detailed geological map of studied area showing sampling locations.

Figure

2.

Representative

photographs

and

photomicrographs

of

Late

Devonian–Carboniferous igneous rocks from the eastern SRM. (a) Outcrop of Devonian alkali feldspar granite; (b) Alkali feldspar granite (15XH2-1); (c) Monzogranite from the Yuejin Pluton; (d) Monzogranite (15XH12-1); (e) Quartz monzodiorite from the Wulidicun Pluton; (f) Quartz monzodiorite (16XH1-1); (g)

ACCEPTED MANUSCRIPT Basaltic andesite from the Heilonggong Formation; (h) Andesite (15XH18-1); (i) Basaltic andesite (15XH18-3); (j) Dacite (15XH18-4); (k) Rhyolite (16XH4-1); (l) Rhyolite in the Zhangguangcailing Complex. Af = alkali feldspar; Bi = biotite; Hb = hornblende; Pl = plagioclase; Q = quartz. .

PT

Figure 3. Cathodoluminescence (CL) images of selected zircon grains from the

RI

analyzed samples. White and red circles represent U–Pb and Lu–Hf analyzed spots,

SC

respectively. Values adjacent to circles are corresponding zircon U–Pb ages and εHf values. 15XH2-1, alkali feldspar granite; 15XH12-1, monzogranite; 15XH18-1,

Figure 4.

MA

quartz monzodiorite; 16XH4-1, rhyolite.

NU

andesite; 15XH19-1, quartz monzodiorite; 16XH1-1, quartz monzodiorite; 16XH2-1,

LA–ICP–MS zircon U–Pb Concordia diagrams for the Late

D

Devonian–Carboniferous igneous rocks from the eastern SRM. 15XH2-1, alkali

PT E

feldspar granite; 15XH12-1, monzogranite; 15XH18-1, andesite; 15XH19-1, quartz monzodiorite; 16XH1-1, quartz monzodiorite; 16XH2-1, quartz monzodiorite;

CE

16XH4-1, rhyolite.

AC

Figure 5. Plots of total alkalis versus SiO2 (TAS) (a), A/NK versus A/CNK (b), Fe* versus SiO2 (c), and (K2O + Na2O – CaO) versus SiO2 (d). A/CNK = molar Al2O3/(CaO + K2O + Na2O); A/NK = molar Al2O3/(K2O + Na2O); Fe* = FeOT/(FeOT + MgO). The data of middle Devonian volcanic rocks are from Meng et al. (2011). A-type granite field is after Frost et al. (2001).

Figure 6. Chondrite-normalized REE and primitive mantle-normalized spider

ACCEPTED MANUSCRIPT diagrams for the Late Devonian–Carboniferous igneous rocks from the eastern SRM. Chondrite and primitive-mantle values are from Boynton (1984) and Sun and McDonough (1989), respectively.

Figure 7. Binary plots showing the compositional variation of Carboniferous igneous

RI

PT

rocks from the eastern SRM.

SC

Figure 8. Plot of zircon U–Pb ages versus εHf values for the Paleozoic igneous rocks from the eastern SRM. The gray circles represent literature data taken from Meng et

NU

al. (2011), Wang et al. (2012a), Wang et al. (2017) and Yu et al. (2013).

MA

Figure 9. Simplified tectonic models for the late Paleozoic evolution of the eastern

AC

CE

PT E

D

SRM and the adjacent JM.

ACCEPTED MANUSCRIPT

Tabel 1 Sample locations and mineral compositions of the Late Devonian-Carboniferous igneous rocks within the eastern SRM Main mineral assemble (vol %)

15XH12

15XH19

16XH1

45°29′58

128°16′56

″

″

45°39′49

129°31′37

″

″

44°55′33

129°12′57

″

″

44°57′37

129°11′16

″

″

Location

44°58′8″

″

2

Yuejin Pluton

monzogranite

35

30

30

3

2

Wulidicun Pluton

quartz monzodiorite

5

45

25

10

9

1

Wulidicun Pluton

quartz monzodiorite

10

50

25

8

5

2

15

50

20

4

10

1

44°54′10 15XH18-4

″ 44°54′10

15XH18-6

″

Heilonggong Formation

129°10′36

Heilonggong Formation

″ 129°10′36 ″

44°57′38 ″ 45°58′11 HDY3

″

129°6′53″

trachyandesite

10

90

basaltic trachyandesite

10

90

dacite

5

10

85

Heilonggong Formation

dacite

5

10

85

rhyolite

15

25

rhyolite

10

Heilonggong Formation

PT E

16XH4

quartz monzodiorite

5

55

129°15′42 ″

Zhangguangcailing Complex

CE

Note: Af = alkali feldspar; AM = accsessory minerals; Bi = biotite; G = groudmass; Hb = hornblende; Pl = plagioclase; Q = quartz.

AC

G

Heilonggong Formation

129°10′36 ″

AM

3

NU

44°54′10 15XH18-3

Hb

55

129°10′36 ″

Bi

5

MA

″

Af

35

D

44°54′10 15XH18-1

Pl

alkali feldspar granite

Wulidicun Pluton

″

Q Yanshou Pluton

129°10′18 16XH2

Lithology

PT

15XH2

Longitude/E

RI

Latitude/N

SC

Sample

90

ACCEPTED MANUSCRIPT Research highlights · 366 Ma A-type granites and ~320 Ma intermediate–felsic rocks are identified. · Late Devonian–Carboniferous rocks formed in a post-collisional extensional setting.

AC

CE

PT E

D

MA

NU

SC

RI

PT

· Crustal accretion in the SRM occurred during the Neoproterozoic–early Paleozoic.

Figure 1

Figure 2

Figure 3

Figure 4

Figure 5

Figure 6

Figure 7

Figure 8

Figure 9