Canadian Journal of Earth Sciences

Geochronology, geochemistry, and Hf isotopic compositions of Early Permian syenogranite and diabase from the northern Great Xing’an Range, NE China: petrogenesis and tectonic implications

Journal: Canadian Journal of Earth Sciences

Manuscript ID cjes-2019-0200.R1

Manuscript Type: Article

Date Submitted by the 06-Apr-2020 Author:

Complete List of Authors: Sun, Yonggang; Jilin University Li, Bile; Jilin University Feng-Yue, DraftSun; College of Earth Sciences, Jilin University Ding, Qing-feng; Jilin University, College of Earth Sciences Qian, Ye; Jilin University Li, Liang; Yunnan University Xu, Qinglin; Shandong University of Science and Technology Li, Yujin; Jilin University

Early Permian, syenogranite, diabase, post-collisional extensional Keyword: setting, Xiaokele, northern Great Xing’an Range

Is the invited manuscript for consideration in a Special Not applicable (regular submission) Issue? :

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1 Geochronology, geochemistry, and Hf isotopic compositions of Early Permian

2 syenogranite and diabase from the northern Great Xing’an Range, NE China:

3 petrogenesis and tectonic implications

4

5 Yong-gang Suna, b, Bi-le Lia, *, Feng-yue Suna, Qing-feng Dinga, Ye Qiana, c, Liang

6 Lid, Qing-lin Xue, Yu-jin Lia, c

7

8 a. College of Earth Sciences, Jilin University, Changchun 130061, China

9 b. Geological Survey Institute of Jilin Province, Changchun 130102, China 10 c. Key Laboratory of Mineral ResourcesDraft Evaluation in Northeast Asia, Ministry of Land and 11 Resources, Changchun 130061, China

12 d. School of Resource Environment and Earth Science, Yunnan University, Kunming 650500,

13 China

14 e. College of Earth Science and Engineering, Shandong University of Science and

15 Technology, Qingdao 266590, China

16

17 *Corresponding author: Tel: 86-13353277179

18 E-mail: [email protected]

19

20 E-mail addresses: [email protected] (Y.-G. Sun)

21 [email protected] (B.-L. Li)

22 [email protected] (F.-Y. Sun)

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23 [email protected] (Q.-F. Ding)

24 [email protected] (Y. Qian)

25 [email protected] (L. Li)

26 [email protected] (Q.-L. Xu)

27 [email protected] (Y.-J. Li)

28

29 Postal address: 2199 Jianshe Street, College of Earth Sciences, Jilin University,

30 Changchun 130061, China

31 32 Abstract Draft 33 Geodynamic evolution in the Late Paleozoic is significant for understanding the final

34 amalgamation of the Central Asian Orogenic Belt (CAOB). No consensus has yet

35 been reached regarding the late Paleozoic geodynamic evolution of the northern Great

36 Xing’an Range (GXR) in Northeast China, the eastern CAOB. Furthermore, late

37 Palaeozoic syenogranite–diabase dyke association is present in the Xiaokele area in

38 northern GXR. It provides an important opportunity to understand the nature of

39 magmatism and the geodynamic evolution during this period. This paper presents new

40 zircon U–Pb ages, zircon Hf isotopic compositions, and geochemical data of

41 whole-rocks for Xiaokele syenogranite and diabase. Zircon U–Pb dating suggests that

42 the Xiaokele syenogranite (292.5 ± 0.9 Ma) and diabase (298.3 ± 1.5 Ma) were

43 emplaced during the Early Permian. The Xiaokele syenogranites have high SiO2

44 contents, low MgO contents, and enriched zircon εHf(t) values, suggesting that their

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45 primary magma was generated by the partial melting of the juvenile crustal material.

46 The Xiaokele diabases have low SiO2 contents, high MgO contents, are enriched in

47 large-ion lithophile elements (LILEs), depleted in high-field-strength elements

48 (HFSEs), and exhibit enriched zircon εHf(t) values. They derived from a lithospheric

49 mantle source that had previously been metasomatized by slab-derived fluids.

50 Combined with previous research results, we believe that the continent–continent

51 collision between the Xing’an and Songliao blocks occurred during the late Early

52 Carboniferous–early Late Carboniferous (330–310 Ma), and the two blocks were

53 transformed into a post-collisional extensional setting during the latest Carboniferous– 54 Early Permian. Draft 55

56 Keywords: Early Permian, syenogranite, diabase, post-collisional extensional setting,

57 Xiaokele, northern Great Xing’an Range.

58

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59 1. Introduction

60 The tectonic evolution of orogenic belts is characterized by changes in the

61 associated magmatic composition (Harris et al., 1986). Post-collisional magmatism, as

62 one of the common characteristics of many orogenic belts in the world, may indicate

63 that the orogenic belt is in an extensional environment (Dewey, 1988) and thus, we

64 can constrain the cessation of collision by studying the petrogenesis of post-collision

65 magmatism (Bonin, 2004; Yang et al., 2007; Hu et al., 2017). As the largest

66 accretionary orogenic belt in the world, the Central Asian Orogenic Belt (CAOB) lies

67 between the Siberian Craton in the north and the Tarim–North China Craton in the

68 south (Fig. 1a; Jahn et al., 2004; DraftLiu et al., 2017). Northeast (NE) China lies in the

69 east of the CAOB, being segmented into the Jiamusi, Songliao, Xing’an, and Erguna

70 Blocks from east to west, and divided by the Mudanjiang–Yilan, Hegenshan–Heihe,

71 and Xinlin–Xiguitu sutures (Fig. 1b; Liu et al., 2017). The Great Xing’an Range

72 (GXR) lies in the west of NE China (Fig. 1a, b) and is an important geological unit for

73 research on the geodynamic evolution of the CAOB (Liu et al., 2017). To date, no

74 consensus has been reached about the late Paleozoic geodynamic evolution of the

75 northern GXR. Some scholars have asserted that the northern GXR was in a

76 subduction setting during the Early Carboniferous–Early Permian (Dong et al., 2016;

77 Yang et al., 2019). Other researches have suggested that the tectonic setting of the

78 northern GXR had transformed into a post-collisional extensional setting by the late

79 Carboniferous (Liu et al., 2017; Zhang et al., 2018; Ma et al., 2019; Ji et al., 2018;

80 Qian et al., 2018a; Shi et al., 2019). These different opinions are attributed to the

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81 absence of a comprehensive understanding of post-collisional magmatism.

82 Granitoid–mafic dyke associations are common in extensional tectonic regimes

83 linked to post-collisional events (Eby, 1992; Yang et al., 2007; Tang et al., 2014). The

84 Xiaokele area lies in the northern GXR (Fig. 1c), and late Palaeozoic granitoid–mafic

85 dyke associations are well exposed in this region, but few have been investigated in

86 detail. It provides a rare opportunity for understanding the nature of magmatism and

87 the geodynamic evolution during this period.

88 This paper presents new zircon U–Pb dating, zircon Hf isotopic, and

89 petrogeochemistry data of the Xiaokele diabase dyke and syenogranite to reveal their 90 source and petrogenesis. CombinedDraft with previous research results, we attempt to 91 constrain the controversial late Paleozoic geodynamic evolution of the northern GXR.

92

93 2. Geological background and sample descriptions

94 The GXR consists of the Erguna, Xing’an, and Songliao Blocks (Fig. 1b; Feng et

95 al., 2015). During the Paleozoic, the GXR was controlled by the evolution of the

96 Paleo-Asian Ocean. Several micro-continental blocks collided and collaged

97 successively with the continuous subduction of the Paleo-Asian Ocean (Şengör et al.,

98 1993; Wu et al., 2011). After the Paleo-Asian Ocean closed, the GXR was

99 superimposed and modified by the Mongol-Okhotsk and Paleo-Pacific tectonic

100 regions during the Mesozoic (Xu et al., 2013; Tang et al., 2016, Sun et al., 2020).

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101 The Erguna Block is clamped between the Mongol–Okhotsk Suture and the

102 Xinlin–Xiguitu Suture (Fig. 1c). The basement of the Erguna Block is composed of

103 Proterozoic (1800–700 Ma) granitoids (Gou et al. 2013; Tang et al. 2013; Ge et al.

104 2015), Neoproterozoic metamorphic supracrustal rocks and granitoids (i.e., the

105 Xinghuadukou, Ergunahe, and Jiageda Groups; IMBGMR, 1991; Sun et al. 2013; Ge

106 et al. 2015). The Erguna Block is mainly composed of Paleozoic and Mesozoic

107 granitic intrusions, Mesozoic volcanic, and clastic rocks (IMBGMR, 1991; Wu et al.,

108 2011; Ge et al., 2015; Tang et al., 2016). In addition, studies on the early Paleozoic

109 post-orogenic granites in the Tahe–Mohe area and blueschist facies metamorphic 110 rocks in Toudaoqiao show that theDraft amalgamation of the Erguna and Xing’an blocks 111 occurred at approximately 500 Ma along the Xinlin–Xiguitu suture zone (Fig. 1c; Ge

112 et al., 2005; Ge et al., 2007; Wu et al., 2011; Zhou et al., 2015).

113 The Xing’an Block is located adjacent to the southeast of the Erguna Block and

114 to the northwest of the Songliao Block (Fig. 1c). The Hegenshan–Heihe suture zone

115 records the closure of the Palaeo-Asian Ocean between the Xing’an and Songliao

116 Blocks (Wu et al., 2011; Liu et al. 2017, Yang et al. 2018). The Xing’an Block is

117 characterized by Paleozoic granitoids and sediments, and voluminous Mesozoic

118 granitoids and related volcanic and sedimentary strata (IMBGMR, 1991; Miao et al.,

119 2004; Ying et al., 2010; Zhang et al., 2010a; Wu et al., 2011). Metamorphic rocks

120 sporadically distributed in the Xing’an Block were previously considered to be

121 “Precambrian basement strata” (i.e., the Xinkailing, Luomahu, Wolegen,

122 Fengshuigouhe, and Zhalantun Groups; IMBGMR, 1996), but more recent studies

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123 have revealed that most of these metamorphic rocks were formed from the Paleozoic

124 to early Mesozoic, and the deformation and metamorphism are related to the Late

125 Paleozoic–Early Mesozoic orogenic processes (Miao et al., 2004; Miao et al., 2007;

126 Xu et al., 2012; Sun et al., 2014; Cui et al., 2015). Therefore, some researchers believe

127 that there may be no Precambrian metamorphic basement in the Xing’an Block (Wu

128 et al. 2011; Miao et al. 2015; Liu et al. 2017). Nevertheless, the recognition of

129 Paleoproterozoic granite gneisses (1.87–1.84 Ga) and Precambrian detrital zircon

130 (2000–580 Ma) in the Zhalantun–Duobaoshan region indicates the presence of a

131 Precambrian basement in the Xing’an Block (Zhou et al. 2014; Li et al., 2019a). In 132 addition, Ordovician island arc Draft assemblages with contemporaneous porphyry Cu 133 mineralization in Duobaoshan have been found in this block (Ge et al., 2007; Wu et

134 al., 2015).

135 The Songliao Block mainly comprises the Lesser Xing’an–Zhangguangcai

136 Range in the east and the Mesozoic Songliao Basin (Feng et al., 2018a). According to

137 the drilling data, the Songliao Basin’s basement rocks are mostly Phanerozoic granites

138 and Paleozoic strata with a weak deformation and metamorphism (Wu et al., 2011).

139 Furthermore, Phanerozoic granites and volcanic rocks are especially well developed

140 in this block, mainly due to Mesozoic magmatism.

141 The samples investigated in this study were collected in the Xiaokele area, which

142 is located in the eastern margin of the Erguna Block (Fig. 1c). It lies ~14 km east of

143 Xinlin town, Heilongjiang Province (Fig. 1c). From old to new, the outcrop stratum in

144 the area includes the Neoproterozoic–Lower Cambrian Jixianggou Formation and

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145 Dawangzi Formation, Upper Jurassic Baiyingaolao Formation, and Quaternary

146 sediments (Fig. 2). The main rock types of the Jixianggou Formation are schist,

147 phyllite, slate, marble, feldspar-bearing quartz siltstone, and metamorphic sandstone.

148 The rock types of the Dawangzi Formation are mainly metamorphosed

149 intermediate-basic lava, interbedded with metamorphosed acidic lava and spotted

150 slate. The Baiyingaolao Formation is composed predominantly of rhyolite and

151 rhyolitic tuff, which rests unconformably on the Jixianggou Formation and Dawangzi

152 Formation. The faults in the area mainly trend NEE and NNW, represented by the

153 Xiaokele River Fault and the Dawusu River Fault, respectively (Fig. 2). The 154 syenogranite predominately situatedDraft in the central part of the area such that it intrudes 155 into the Jixianggou Formation and Dawangzi Formation rocks, was overlain

156 unconformably by the Baiyingaolao Formation. In addition, it was crosscut by Early

157 Cretaceous quartz monzonite (Fig. 2). The diabase dyke, located in the southern part

158 of the area, intruded into the Jixianggou Formation (Fig. 2).

159 Syenogranite and diabase samples were collected from surface exposures. After

160 examination under standard optical microscopy, samples with the weakest weathering

161 degree were selected for zircon U–Pb dating, geochemical, and Hf isotopic analyses.

162 The sample geotraverses are shown in Figure 2. The syenogranite has a

163 medium-coarse-grained texture with a massive structure, which is mainly composed

164 of quartz (20%–25%), plagioclase (20%–25%), alkali feldspar (45%–50%),

165 hornblende (~5%), and biotite (~5%) (Fig. 3a). The diabase has an ophitic texture and

166 massive structure, and mainly consists of euhedral to subhedral plagioclase (55%–

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167 60%), hornblende (30%–35%), clinopyroxene (~5%), and biotite (~5%) (Fig. 3b).

168

169 3. Analytical methods

170 3.1. Zircon U–Pb dating

171 The sorting of zircons was completed at Shangyi Geologic Service Co. Ltd.,

172 Langfang, China. Magnetic and heavy liquid separation methods were adopted after

173 the samples were crushed. Zircons with good crystal shape, no cracks, and no obvious

174 inclusions were handpicked through binocular microscopes. The inner structures of 175 zircons were revealed through cathodeDraft luminescence (CL) microphotographs. Laser 176 ablation–inductively coupled plasma–mass spectrometry (LA–ICP–MS) zircon U–Pb

177 analyses were performed at Yanduzhongshi Geological Analysis Laboratories,

178 Beijing, China, using an Aurora M90 ICP–MS instrument equipped with a New Wave

179 UP 213 LA system. Specific experimental testing procedures were presented by Yuan

180 et al. (2004). Helium was used as the carrier gas. Age calibration was performed using

181 91500 standard zircons as the external standard. The element concentration was

182 calculated using the NIST610 reference standard, and 29Si was used as the interior

183 standard. The samples were analyzed using a laser beam with a diameter of 30 μm.

184 The method of Andersen (2002) was used to correct the results for common lead.

185 Calculations were performed using the ICPMSDataCal program (Liu et al., 2008).

186 Concordia plots and weighted-mean ages were produced using ISOPLOT (Version

187 3.0) (Ludwig, 2003). Table S1 presents the zircon U–Pb isotopic data.

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188

189 3.2. Whole-rock major and trace element compositions

190 Altered surfaces were removed from samples for whole-rock analysis before

191 being smashed to 200 mesh. All whole-rock analyses were undertaken at the Key

192 Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Land and

193 Resources, Jilin University, Changchun, China. Major-element contents were

194 determined using X-ray fluorescence (XRF) spectroscopy on fused glass disks.

195 Trace-element contents were determined by ICP–MS using an Agilent 7500a system

196 after the sample powders were dissolved in HF in Teflon bombs. More detailed 197 analytical procedures were similarDraft to those described by Li et al. (2019b). The 198 accuracy and precision of the analyses were <5% for major elements and <10% for

199 trace elements, as estimated using the international standards BHVO-2 and BCR-2 as

200 well as the national standards GBW07103 and GBW07104. Major- and trace-element

201 data are presented in Table S2.

202

203 3.3. Zircon Hf isotopic analyses

204 Zircon Hf isotopic analyses were performed using a Nepture-plus MC–ICP–MS,

205 coupled with a NewWave UP213 laser-ablation system at Yanduzhongshi Geological

206 Analysis Laboratories, Beijing, China. Instrumental conditions and data acquisition

207 techniques have been reported by Wu et al. (2006). The ablation spots for the Hf

208 isotope analyses were located over the U–Pb age analysis positions on each grain.

209 Ablation pits with a diameter of 30 μm were denudated using a laser with a frequency

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210 of 8 Hz and energy of 16 J/cm2, for 31 s. With the 176Lu/177Hf ratio in zircons being

211 <0.002, the isotopic interference of 176Lu with 176Hf was negligible. The fractionation

212 coefficient of Yb was based on the mean 173Yb/172Yb ratio for each spot and the

213 interference of 176Yb on 176Hf was deduced accordingly. A 173Yb/172Yb ratio of

214 1.35274 was adopted. The zircon standard PLE was measured to correct and monitor

215 Hf isotopic values. Off-line selection and integration of analyte signals and mass bias

216 calibrations were performed using ICPMSDataCal (Liu et al., 2010). A decay constant

217 of 1.867 × 10−11 year−1 was adopted for 176Lu (Soderlund et al., 2004). Detailed data

218 processing has been described by Li et al. (2019c). The zircon Lu–Hf isotopic data are 219 presented in Table S3. Draft 220

221 4. Analytical results

222 4.1. LA–ICP–MS zircon U–Pb geochronology

223 4.1.1. Syenogranite

224 Cathode luminescence (CL) microphotographs demonstrate that the zircons

225 selected from the syenogranite sample (XKL–TW5) are mostly euhedral to subhedral

226 columnar in shape, and the majority exhibit obvious features of concentric and typical

227 magmatic oscillatory zonation (Fig. 4a). The Th and U contents of 26 analytical spots

228 varied from (58–792) to (319–1722) ppm, respectively, and the Th/U ratios were in

229 the range of 0.13–0.58 (Table S1), implying a magmatic origin (Hoskin, 2003). The

230 206Pb/238U ages of 26 analytical spots were 298–288 Ma with a weighted mean age of

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231 292.5 ± 0.9 Ma (MSWD = 0.82; Fig. 5a). This is interpreted as the crystallization age

232 of the syenogranite.

233

234 4.1.2. Diabase

235 CL microphotographs show that most zircons selected from diabase samples

236 (XKL–TW2) are mainly irregular in shape. All zircons display weak oscillatory

237 zoning with no core-rim structure, presenting the characteristics of zircon in basic

238 rocks (Fig. 4b). The Th and U contents of 15 analytical spots varied from (74–636) to

239 (99–543) ppm, respectively, and the Th/U ratios were in the range of 0.36–1.62 (Table 240 S1), implying a magmatic origin (Hoskin,Draft 2003). The 206Pb/238U ages of 15 analytical 241 spots were 301–295 Ma with a weighted mean age of 298.3 ± 1.5 Ma (MSWD = 0.40;

242 Fig. 5b). This is interpreted as the crystallization age of the diabase.

243

244 4.2. Major and trace element geochemistry

245 4.2.1. Syenogranite

246 The eight syenogranite samples contained 71.8–73.1 wt. % SiO2, 13.3–14.0

247 wt. % Al2O3, 3.65–4.02 wt. % Na2O, 4.95–5.43 wt. % K2O, 8.80–9.17 wt. % (Na2O +

T 248 K2O), 0.280–0.598 wt. % CaO, 0.275–0.344 wt. % TiO2, 2.08–2.45 wt. % Fe2O3 ,

249 0.410–0.768 wt. % MgO, and Mg# = 25.8–39.0 (Table S2). The syenogranite samples

250 belong to the subalkaline series (Fig. 6a) and can be classified as high-K calc-alkaline

251 series (Fig. 6b). A/CNK ratios of 1.05–1.10 display weakly peraluminous

252 characteristics (Fig. 6c).

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253 In the chondrite-normalized REE pattern (Fig. 7a), the syenogranite samples

254 display depleted heavy rare-earth elements (HREEs) relevant to light rare-earth

255 elements (LREEs) as well as high (La/Yb)N (5.7–13.9) and obvious negative Eu

256 anomalies (Eu/Eu* = 0.466–0.732). In the primitive mantle-normalized spider diagram

257 (Fig. 7b), the syenogranite samples are enriched in large-ion lithophile elements

258 (LILEs; e.g., Rb, Th, U, K, and La), and depleted in Ba, Nb, Sr, P, and Ti.

259

260 4.2.2. Diabase

261 The eight diabase samples contained 48.2–49.1 wt. % SiO2, 14.9–16.4 wt. %

262 Al2O3, 2.98–3.77 wt. % Na2O, 0.89–2.18Draft wt. % K2O, 4.22–5.79 wt. % (Na2O + K2O), T 263 6.63–8.24 wt. % CaO, 1.67–2.36 wt. % TiO2, 10.3–11.6 wt. % Fe2O3 , 5.82–7.04

264 wt. % MgO, and Mg# = 51.6–55.6 (Table S2). The samples mainly belong to the

265 alkaline series (Fig. 6a).

266 In the chondrite-normalized REE pattern (Fig. 7c), the diabase samples display

267 depleted HREEs relative to LREEs, and no Eu anomalies (Eu/Eu* = 0.844–0.987). In

268 the primitive mantle-normalized spider diagram (Fig. 7d), the diabase samples are

269 enriched in LILEs (e.g., Rb, Ba, and K) and depleted in high-field strength elements

270 (HFSEs; e.g., Nb, Ta, Zr, Hf, and Ti).

271

272 4.3. Zircon Hf isotopes

273 Sixteen analyses of zircons were conducted from syenogranite samples (XKL–

274 TW5) yielding 176Yb/177Hf ratios of 0.023158–0.072423 and 176Lu/177Hf ratios of

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275 0.000907–0.002436. The 176Hf/177Hf ratios are 0.282633–0.282770, which

276 corresponds to εHf(t) values of 1.14–6.17 (Fig. 8). The TDM2 model ages range from

277 1236 to 917 Ma (Table S3). Fourteen analyses of zircons were conducted from the

278 diabase samples (XKL–TW2) yielding 176Yb/177Hf ratios of 0.026121–0.167502 and

279 176Lu/177Hf ratios of 0.000885–0.005039. The 176Hf/177Hf ratios are 0.282633–

280 0.282809 with εHf(t) values of 1.46–6.99 (Fig. 8). The TDM1 model ages range from

281 880 to 661 Ma (Table S3). The ɛHf(t) values fall into the area between the chondrite

282 evolution line and the depleted mantle line (Fig. 8a), which remains close to zircons

283 from the Phanerozoic magmatic rocks in the eastern CAOB (Fig. 8a; Yang et al., 284 2006). Draft 285

286 5. Discussion

287 5.1. Petrogenesis of the Xiaokele syenogranite

288 Based on their protolith, granite is usually classified into A-, M-, S-, and I-type

289 (Chappell and White, 1992). The Xiaokele syenogranite has high concentrations of

290 K2O (4.95–5.43 wt. %), which is different from the M-type granites with low K2O

291 content (< 1 wt. %; Bonin, 2007). S-type granites are usually strongly peraluminous

292 (A/CNK > 1.1; Chappell and White, 1974; Clemens, 2003), but the Xiaokele

293 syenogranite is weakly peraluminous (A/CNK < 1.1; A/NK > 1.0). Although the

294 Xiaokele syenogranite has geochemical characteristics similar to those of typical

295 A-type granites such as enrichment in Rb, U, and Th in addition to depletion in Ba,

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296 Sr, P, Ti, and Eu (Fig. 7a, b; Whalen et al., 1987; Eby, 1990; Li et al., 2014b; Li et al.,

297 2018a; Li et al., 2018b; Girei et al., 2019), the following evidence supports that they

298 are I-type granites rather than A-type granites. The P2O5 content decreases with

299 increasing SiO2 content (Fig. 9a) and the Th content increases with an increase in the

300 Rb content (Fig. 9b), showing the tendency of I-type granites (Chappell, 1999). The

301 existence of hornblende, biotite, and the absence of muscovite, garnet, and cordierite

302 in the Xiaokele syenogranite also suggests that they were I-type granites.

303 The Xiaokele syenogranite displays high values of the differentiation index (DI =

304 92.0–93.7), implying that the magmas that generated the Xiaokele syenogranite were 305 highly fractionated (Wu et al., 2003).Draft In addition, data for the Xiaokele syenogranite 306 samples plot in the highly fractionated I-type granite domain of Wu et al. (2003) in

307 Figure 9c–f. This result suggests that the Xiaokele syenogranite belongs to highly

308 fractionated I-type granites.

309 According to previous data, the highly fractionated I-type granites may have the

310 following two types of genesis: (1) partial melting of crustal materials (Chappell,

311 1999; Chappell et al., 2012) or (2) fractional crystallization of mantle-derived mafic

312 parental magmas (Cawthorn and Brown, 1976; Wyborn et al., 2001). There is a

313 question of whether there is a genetic relationship between the Xiaokele syenogranite

314 and the diabase. We found the following evidence: (1) the composition range of the

315 Xiaokele syenogranite is narrow, and there is a distinct compositional gap between

316 syenogranite and diabase (Fig. 6a); (2) the coexisting diabase in Xiaokele occurs in

317 very small volumes, and (3) the fractional crystallization of mantle-derived mafic

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318 magmas is unlikely to produce silicic magmas with such high SiO2 contents (>

319 71 wt. %). We therefore conclude that the Xiaokele syenogranite cannot directly

320 generate via the fractional crystallization of mantle-derived mafic parental magmas

321 (the Xiaokele diabase) and that it has an independent origin. The Xiaokele

322 syenogranites are enriched in LILEs (e.g., Rb, Th, U, K, La) and depleted in Ba, Nb,

323 Sr, P, and Ti, suggesting that they are crust-derived granites (Sun et al., 2017; Kong et

324 al., 2018). Some trace element ratios (e.g., Nb/Ta, Zr/Hf, and Th/U) change little

325 during magmatic evolution, so they are often used as indicators of magmatic origin

326 (e.g., Li et al., 2018c). The Xiaokele syenogranites have relatively low Nb/Ta (11.3– 327 16.5, mean = 13.9), Zr/Hf (34.8–37.9,Draft mean = 36.4), and Th/U ratios (4.3–7.6, mean = 328 5.9; Table S2), which are close to the average crustal compositions (Nb/Ta = 11.4,

329 Zr/Hf = 33, and Th/U = 4; Taylor and Mclennan, 1985). This further demonstrates

330 that magma originates from a crustal source. We conclude that partial melting played

331 a leading role in the formation of the magmas according to the discriminant diagrams

332 of magmatic evolution (Fig. 9g–i). The zircons in the syenogranites have positive

333 εHf(t) values ranging from 1.14 to 6.17, which vary between the values of depleted

334 mantle and CHUR (Fig. 8), and yield TDM2 model ages of 1236–917. Therefore, we

335 consider that the primary magma of the Xiaokele syenogranite was generated by the

336 partial melting of the juvenile crustal material. This implies that the Erguna Block

337 experienced remarkable crustal growth during the Meso-Neoproterozoic, which is

338 consistent with previous research results (Zhang et al., 2008a; Gou et al., 2013).

339

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340 5.2. Petrogenesis of the Xiaokele diabase

341 Magmatic rocks derived from depleted mantle usually have extremely high εHf(t)

342 values (> 10) (Zhong et al., 2017; Yan et al., 2019). However, the Xiaokele diabase

343 has zircon U–Pb ages of 301–295 Ma, εHf(t) values of 1.46–6.99, and TDM1 model

344 ages of 880–661 Ma. Previous works believed that these characteristics could be

345 defined as the depleted mantle being influenced by enriched components such as

346 magmas from a depleted mantle source that was metasomatized by slab-derived fluids

347 (Gill, 1981; Grove et al., 2003; Zhong et al., 2017; Yang et al., 2020), or a depleted

348 mantle source influenced by crustal contamination and slab-derived fluid 349 metasomatism (Li et al., 2019d; Draft Yan et al., 2019; Yan et al., 2020). Although the 350 depletion in Nb–Ta of the Xiaokele diabase implies that some crustal contamination

351 might occur (Rudnick and Gao, 2003), several lines of evidence indicate that crustal

352 contamination has no obvious effect on the formation of the Xiaokele diabase. (1)

# 353 Low SiO2 (48.2–49.1 wt. %) contents, high MgO (5.82–7.04 wt. %) contents, Mg

354 values (51.6–55.6), Cr (145–195 ppm) contents, and Ni (69.9–80.7 ppm) contents of

355 the Xiaokele diabase (Table S2) suggest that they are not significantly contaminated

356 by the crust contamination. (2) All the Xiaokele diabase samples display negative

357 anomalies of Zr–Hf (Fig. 7d), which are different from those generated by crustal

358 contamination because crustal materials are obviously enriched in Zr and Hf. (3) No

359 crustal xenoliths, xenocrysts, or inherited zircon with ancient zircon U–Pb ages have

360 been found in the Xiaokele diabase samples, also indicating that crustal contamination

361 is minor (Li et al., 2019e). (4) Both crustal contamination and slab melting can lead to

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362 Nb and Ta depletions (Sun and McDonough, 1989). When combining this with the

363 discussion below, we consider that the depletion in Nb–Ta was mainly inherited from

364 their source, rather than from crustal contamination (Qian et al., 2018b). (5)

365 Moreover, the range of zircon εHf(t) values (1.46–6.99) is smaller and much higher

366 than that of typical crustal contamination. Therefore, we conclude that crustal

367 contamination contributes little for the Xiaokele diabase, so their geochemical

368 compositions can be used to research their mantle source.

369 Because there was no significant crustal contamination in the samples, we

370 suggest that the mantle source was most likely metasomatized by slab-derived fluids. 371 The Xiaokele diabase are enrichedDraft in LREEs and LILEs (e.g., Rb, Ba, and K) and 372 depleted in HFSEs (e.g., Nb, Ta, Zr, Hf, and Ti), which indicates arc geochemical

373 affinities but different from those of N-MORB sourced from asthenospheric mantle

374 (Fig. 7a, b; Pearce et al., 1984; Crawford et al., 1987; Davidson, 1987). The high

375 La/Nb ratios (2.27–2.70) and La/Ta ratios (50.6–56.8) in the Xiaokele diabase also

376 indicate the origin from the lithospheric mantle (La/Nb > 1, La/Ta > 20; Fitton et al.,

377 1988, Thompson and Morrison, 1988) rather than the asthenospheric mantle (La/Nb <

378 1, La/Ta ≈ 10; Fitton et al., 1988; Thompson and Morrison, 1988). Moreover, data for

379 the Xiaokele diabase samples are located above the MORB–OIB array in the Nb/Yb

380 vs. Th/Yb diagram, plot in the field of mafic melts derived from subduction-modified

381 lithospheric mantle (Fig. 10a; Leat et al., 2002), suggesting that they were derived

382 from a source enriched by subduction-related metasomatism. Sediment-derived melts

383 as well as slab-derived fluids could be identified effectively by trace element ratios

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384 (Th/Nb, Ba/Th, Th/Yb, Ba/La). The Th/Nb vs. Ba/Th and Th/Yb vs. Ba/La diagrams

385 indicate that the Xiaokele diabase displays characteristic trends of a source modified

386 by slab-derived fluids (Fig. 10b, c). Moreover, the Xiaokele diabase samples show a

387 trend towards the continental lithospheric mantle (CLM) field in the La/Nb vs. La/Ba

388 diagram (Fig. 10d), which also suggests a lithospheric mantle source.

389 In summary, we consider that the Xiaokele diabase was derived from a

390 lithospheric mantle source that had previously been metasomatized by slab-derived

391 fluids.

392 393 5.3. Implications for the late PaleozoicDraft tectonic evolution of the northern GXR 394 It has been widely accepted that the Erguna and Xing’an Blocks amalgamated at

395 approximately 500 Ma along the Xinlin–Xiguitu suture. In contrast, accretionary

396 prisms and ophiolites are poorly exposed within the Hegenshan–Heihe suture zone,

397 and the relatively intact ophiolites are only preserved in the Hegenshan area (Fig. 1c).

398 As a result, the amalgamation timing of the Xing’an and Songliao blocks remains

399 controversial. The main conclusions regarding this timing are as follows: the Late

400 Silurian–Devonian (Su, 1996; Yue et al. 2001), Late Devonian–Early Carboniferous

401 (Badarch et al., 2002; Tang et al., 2011), late Early Carboniferous (Zhao et al., 2010;

402 Liu et al., 2012; Cui et al., 2013), early Late Carboniferous (Li et al., 2014a; Yang et

403 al., 2018), late Early Carboniferous–early Late Carboniferous (Liu et al., 2017; Zhang

404 et al., 2018; Ji et al., 2018), pre-Permian (Sun et al., 2001; Wu et al. 2002; Zhang et

405 al., 2013), Late Permian and earliest Triassic (Dong et al., 2016; Yang et al., 2019),

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406 Triassic (Chen et al., 2000; Miao et al., 2004), and Early Cretaceous (Nozaka and Liu,

407 2002).

408 By reviewing previous data in this region, Liu et al. (2017) concluded that two

409 subduction-related magmatic arc belts along the eastern margin of the Xing’an Block

410 were early Paleozoic (ca. 480–420 Ma) and late Paleozoic (ca. 360–330 Ma). During

411 the two magmatic arc events (ca. 420–360 Ma), the Devonian sediments were

412 deposited in the Xing’an Block without magmatic activity (Liu et al., 2017). The

413 results show that the subduction of the Paleo-Asian Ocean continued to occur during

414 the Late Devonian–Early Carboniferous (Liu et al., 2017). The recently reported Early 415 Carboniferous forearc basalts (∼335.6Draft Ma) recorded in the Diyanmiao ophiolite zone 416 near the Hegenshan area (Li et al., 2020) further show that the Hegenshan ophiolites

417 related to the subduction of the Paleo-Asian Ocean should be emplaced in the Early

418 Carboniferous. This evidence demonstrates that the amalgamation of the Xing’an and

419 Songliao blocks did not occur before the Early Carboniferous. After the Early

420 Carboniferous magmatic arc (360–330 Ma), widespread low-Mg adakitic magmatism

421 with zircon U–Pb ages of 330–310 Ma has been identified in the Hailaer Basin

422 (Zhang et al., 2010b) and western margin of the Songliao Block (Li et al., 2014a), as

423 well as in Yakeshi (Zhang et al., 2018), Zhalantun (Zhang et al., 2016), Manzhouli

424 (Gou et al., 2013), and Lizishan and Dabeigou areas (Ji et al., 2018), they were

425 thought to be derived from magmas produced by the partial melting of a juvenile

426 region of thickened lower crust. The regional stratigraphic data showed that early

427 Carboniferous and late Carboniferous are dominated by marine and terrestrial strata,

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428 respectively (HBGMR, 1993; IMBGMR, 1996), and the depositional sequence of the

429 Serpukhovian, Bashkirian, and Moscovian stages disappeared (IMBGMR, 1996),

430 indicating that the main body of the GXR experienced crustal uplift and erosion

431 during 326–311 Ma (Zhao et al., 2010). Moreover, Liégeois et al. (1998) believed that

432 vast quantities of high-K calc-alkaline magmatism were produced during a

433 post-collisional period, and the magma compositions were converted to shoshonitic

434 compositions at the end of this period. The Late Devonian–Early Carboniferous rocks

435 in the northern GXR mainly belong to middle-K to high-K calc-alkaline series,

436 whereas the latest Carboniferous–Early Permian rocks mainly exhibit high-K 437 calc-alkaline to shoshonitic geochemicalDraft features (Fig. 6b). It is very likely that the 438 latest Carboniferous–Early Permian rocks were generated in a post-collisional setting,

439 as discussed below. Therefore, this evidence suggests that the late Early

440 Carboniferous–early Late Carboniferous magmatism (330–310 Ma) were associated

441 with contemporaneous continent–continent collision between the Xing’an and

442 Songliao blocks. In recent years, the voluminous latest Carboniferous–Early Permian

443 A-type granites (ca. 307–282 Ma; Wu et al., 2002; Sui et al., 2009; Gou et al., 2018;

444 Yang et al., 2018; Shi et al., 2019; Zhang et al., 2019) and bimodal volcanic rocks (ca.

445 307–279 Ma; Zhao et al., 2010; Meng et al., 2011; Zhang et al., 2008b; Xin et al.,

446 2011; Zhang et al., 2017) are recognized in the GXR. This indicates that the two

447 blocks were transformed into a post-collisional extensional setting during the latest

448 Carboniferous–Early Permian. However, the early Permian post-collisional

449 extensional setting seems to contradict the conclusion that the Xiaokele diabase was

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450 derived from a lithospheric mantle source that had previously been metasomatized by

451 slab-derived fluids (see section 5.2). Some researchers have studied the

452 contemporaneous magmatic rocks with similar geochemical features in the northern

453 GXR and concluded that they show typical arc-like signatures and were in a

454 subduction setting during the Early Carboniferous–Early Permian (Dong et al., 2016;

455 Yang et al., 2019). Many researchers, however, show that igneous rocks with arc-like

456 signatures do not always mean a subduction setting (e.g., Pearce et al., 1990;

457 Peccerillo, 1998; Aldanmaz et al., 2000; Chen et al., 2009; Zhang et al., 2011).

458 Instead, they may be related to magma sources enriched by subduction events before 459 the collision (Pearce et al., 1990;Draft Peccerillo, 1998; Aldanmaz et al., 2000). Some 460 examples are the Early Permian post-collisional mafic volcanic rocks from the NW

461 Inner Mongolia of China (Zhang et al., 2011), the late Cenozoic post-collisional

462 basalts from the western Anatolia in Turkey (Aldanmaz et al., 2000), the

463 Plio-Pleistocene post-collisional basalts from the Northern Taiwan Volcanic Zone

464 (Wang et al., 2004), and the middle Silurian Akechukesai mafic-ultramafic complex

465 in the eastern Kunlun area of the northern Tibet Plateau, west China (Yan et al.,

466 2020).

467 In summary, the continent–continent collision between the Xing’an and Songliao

468 blocks occurred during the late Early Carboniferous–early Late Carboniferous (330–

469 310 Ma), and the two blocks were transformed into a post-collisional extensional

470 setting during the latest Carboniferous–Early Permian.

471

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472 6. Conclusions

473 (1) Zircon U–Pb dating shows that Xiaokele syenogranite (292.5 ± 0.9 Ma) and

474 diabase (298.3 ± 1.5 Ma) were emplaced during the Early Permian.

475 (2) The Xiaokele syenogranite belongs to highly fractionated I-type granites. The

476 primary magma of the Xiaokele syenogranite was generated by partial melting of the

477 Meso-Neoproterozoic juvenile crustal material. The Xiaokele diabase was derived

478 from a lithospheric mantle source that had previously been metasomatized by

479 slab-derived fluids.

480 (3) The continent–continent collision between the Xing’an and Songliao blocks

481 occurred during the late Early Carboniferous–earlyDraft Late Carboniferous (330–310

482 Ma), and the two blocks were transformed into a post-collisional extensional setting

483 during the latest Carboniferous–Early Permian.

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484 Acknowledgements

485 We would like to thank staffs of the Qiqihaer Institute of Geological Exploration,

486 Heilongjiang, China for sample collection. This research was funded by the National

487 Natural Science Foundation of China (41272093), the National Key R&D Program of

488 China (2017YFC0601304), Natural Science Foundation of Jilin Province

489 (No.20180101089JC), Key Projects of Science and Technology Development Plan of

490 Jilin Province (No.20100445), Self-determined Foundation of Key Laboratory of

491 Mineral Resources Evaluation in Northeast Asia, Ministry of Natural Resources 492 (DBY-ZZ-19-04), and the HeilongjiangDraft Research Project of Land and Resources 493 (201605 and 201704).

494

495 Declaration of interest

496 We declare no conflicts of interest in this study.

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795 age and nature of ‘Precambrian metamorphic rocks’ in the Xing’an block of Northeast

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821 the genesis of post-collisional magmatism and the geodynamic evolution of the

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823 Whalen, J. B., Currie, K. L., Chappell, B. W., 1987. A-Type Granites: Geochemical

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824 Characteristics, Discrimination and Petrogenesis. Contributions to Mineralogy and

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826 Wu, F. Y., Jahn, B. M., Wilde, S. A., et al., 2003. Highly fractionated I-type granites

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829 granitoids in northeastern China. Journal of Asian Earth Sciences, 41(1): 1–30.

830 Wu, F. Y., Sun, D. Y., Li, H. M., et al., 2002. A-type granites in northeastern China:

831 age and geochemical constraints on their petrogenesis. Chemical Geology, 187(1):

832 143–173. 833 Wu, G., Chen, Y. C., Sun, F. Y.,Draft et al., 2015. Geochronology, geochemistry, and 834 Sr-Nd-Hf isotopes of the early Paleozoic igneous rocks in the Duobaoshan area, NE

835 China, and their geological significance. Journal of Asian Earth Sciences, 97: 229–

836 250.

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838 in high temperature granites from the Lachlan Fold Belt. Australian Journal of Earth

839 Sciences, 48: 531–541.

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841 geochronology study on the Baoligaomiao Formation in the East Ujimqin County,

842 Inner Mongolia. Geological Survey and Research, 34(1): 1–9 (in Chinese with

843 English abstract).

844 Xu, M. J., Xu, W. L., Wang, F., et al., 2012. Age, association and provenance of the

845 “Neoproterozoic” Fengshuigouhe Group in the northwestern Lesser Xing’an Range,

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846 NE China: Constraints fromzircon U–Pb geochronology. Journal of Earth Science,

847 23: 786–801.

848 Yan, J. M., Sun, F. Y., Li, B. L., et al., 2020. Geochronological, geochemical, and

849 mineralogical characteristics of the Akechukesai-I mafic–ultramafic complex in the

850 eastern Kunlun area of the northern Tibet Plateau, west China: Insights into ore

851 potential. Ore Geology Reviews, 121: 103468.

852 Yan, J. M., Sun, F. Y., Li, L., et al., 2019. A slab break-off model for mafic–

853 ultramafic igneous complexes in the East Kunlun Orogenic Belt, northern Tibet:

854 insights from early Palaeozoic accretion related to post-collisional magmatism. 855 International Geology Review, 61(10):Draft 1171–1188. 856 Yang, D. G., Sun, D. Y., Gou, J., et al., 2018. Petrogenesis and tectonic setting of

857 Carboniferous hornblende gabbros of the northern Great Xing’an Range, NE China:

858 Constraints from geochronology, geochemistry, mineral chemistry, and zircon Hf

859 isotopes. Geological Journal, 53(5): 2084–2098.

860 Yang, H., Ge, W. C., Ji, Z., et al., 2019. Late Carboniferous to early Permian

861 subduction-related intrusive rocks from the Huolongmen region in the Xing’an Block,

862 NE China: new insight into evolution of the Nenjiang–Heihe suture. International

863 Geology Review, 61(9): 1071–1104.

864 Yang, H., Xu, W. L., Sorokin, A. A., et al., 2020. Geochronology and geochemistry of

865 Neoproterozoic magmatism in the Bureya Block, Russian Far East: Petrogenesis and

866 implications for Rodinia reconstruction. Precambrian Research, 342: 105676.

867 Yang, J. H., Sun, J. F., Chen, F. K., et al., 2007. Sources and petrogenesis of late

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868 triassic dolerite dikes in the Liaodong Peninsula: implications for post-collisional

869 lithosphere thinning of the Eastern North China Craton. Journal of Petrology, 48(10):

870 1973–1997.

871 Yang, J. H., Wu, F. Y., Shao, J. A., et al., 2006. Constrains on the timing of uplift of

872 the Yanshan Fold and Thrust Belt, north China. Earth and Planetary Science Letters,

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875 geochemical investigation of the late Mesozoic volcanic rocks from the Northern

876 Great Xing’an Range and their tectonic implications. International Journal of Earth 877 Sciences, 99: 357–378. Draft 878 Yuan, H. L., Gao, S., Liu, X. M., et al., 2004. Accurate U–Pb age and trace element

879 determinations of zircon by laser ablation-inductively coupled plasma-mass

880 spectrometry. Geostandards and Geoanalytical Research, 28: 353–370.

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882 Inner Mongolia orogens and its implications for the palinspastic reconstruction of

883 north China. in Hendrix, M.S., Davis, G.A. eds., Paleozoic and Mesozoic tectonic

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885 Boulder, Colorado. Geological Society of America Memoir, 194: 101–116.

886 Zhang, C., Liu, Z. H., Xu, Z. Y., et al., 2013. Characteristics and genesis of the Wuyi

887 Forestry Center granite in the Da Hinggan Mountains. Geological Bulletin of China,

888 32(2–3): 365–373 (in Chinese with English Abstract).

889 Zhang, F. Q., Chen, H. L., Cao, R. C., et al., 2010b. Discovery of Late Paleozoic

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890 adakite from the basement of the Hailaer basin in NE China and its geological

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892 Abstract).

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894 volcanic rocks in the Great Xing’an Range, northeastern China: implications for

895 subduction-induced delamination. Chemical Geology, 276(3): 144–165.

896 Zhang, L., Liu, Y. J., Shao, J., et al., 2019, Early Permian A-type Granites in the

897 Zhangdaqi Area, Inner Mongolia, China and Their Tectonic Implications. Acta

898 Geologica Sinica, 93(5): 1300–1316. 899 Zhang, X. H., Wilde, S. A., Zhang,Draft H. F., et al., 2011. Early Permian high-K 900 calc-alkaline volcanic rocks from NW Inner Mongolia, North China: geochemistry,

901 origin and tectonic implications. Journal of the Geological Society, London, 168:

902 525–543.

903 Zhang, X. H., Zhang, H. F., Tang, Y. J., et al., 2008b. Geochemistry of Permian

904 bimodal volcanic rocks from Central Inner Mongolia, North China: implication for

905 tectonic setting and Phanerozoic continental growth in Central Asian Orogenic Belt.

906 Chemical Geology, 249(3–4): 262–281.

907 Zhang, Y. J., Wu, X. W., Yang, Y. J., et al., 2016. Discovery and geological

908 significance of adakitic rocks in the Late Paleozoic Gegenaobao Formation in

909 Zhalantun area, Middle Daxinganling Mountains. Geology and Resources, 25(3):

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911 Zhang, Y. L., Ge, W. C., Liu, X. M., et al., 2008a. Isotopic characteristics and its

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912 significance of the Xinlin Town Pluton, Great Hinggan Mountains. Journal of Jilin

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914 Abstract).

915 Zhang, Y., Pei, F. P., Wang, Z. W., et al., 2018. Late Paleozoic tectonic evolution of

916 the central great Xing’an Range, Northeast China: Geochronological and geochemical

917 evidence from igneous rocks. Geological Journal, 53(1): 282–303.

918 Zhang, Z. C., Chen, Y., Li, K., et al., 2017. Geochronology and geochemistry of

919 Permian bimodal volcanic rocks from Central Inner Mongolia, China: Implications for

920 the late Palaeozoic tectonic evolution of the south-eastern Central Asian Orogenic 921 Belt. Journal of Asian Earth SciencesDraft, 135, 370–389. 922 Zhao, S. F., Wang, C. S., Sun, J. G., et al., 2016. Zircon U–Pb ages, geochemical

923 characteristics of alkali-feldspar granite in Xiaomoeke area in Great Xing’an Range

924 and their geological implications. Global Geology, 35(2): 324–335+347.

925 Zhao, Z., Chi, X. G., Pan, S. Y., et al., 2010. Zircon U-Pb LA-ICP-MS dating of

926 Carboniferous volcanics and its geological significance in the northwestern Lesser

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928 Abstract).

929 Zhong, S. H., Feng, C. Y., Seltmann, R., et al., 2017. Middle Devonian volcanic rocks

930 in the Weibao Cu–Pb–Zn deposit, East Kunlun Mountains, NW China: Zircon

931 chronology and tectonic implications. Ore Geology Reviews, 84: 309–327.

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932 Zhou, J. B., Wang, B., Wilde, S. A., et al., 2015. Geochemistry and U–Pb zircon

933 dating of the Toudaoqiao blueschists in the Great Xing’an Range, northeast China,

934 and tectonic implications. Journal of Asian Earth Sciences, 97: 197–210.

935 Zhou, J. B., Wang, B., Zeng, W. S., et al., 2014. Detrital Zircon U–Pb dating of the

936 Zhalantun metamorphic complex and its tectonic implications, Great Xing’an, NE

937 China. Acta Petrologica Sinica, 30(7): 1879–1888 (in Chinese with English abstract).

Draft

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938 Figure captions

939 Figure 1. (a) Schematic tectonic map of the Eurasian continent showing the major

940 tectonic units and the location of Fig. 1b (modified after Kröner et al., 2014; Liu et al.,

941 2017). (b) Tectonic division of northeast China showing the location of Fig. 1c

942 (modified after Liu et al., 2017). (c) Schematic geological map of the Great Xing’an

943 Range and its adjacent areas, showing the main tectonic units and the distribution of

944 Paleozoic magmatic rocks (modified after Liu et al., 2017).

945 Permissions for this figure are not required from the original source(s)/copyright 946 holder(s) to publish. Coreldraw X8Draft was used to create the map. 947

948 Figure 2. Geological map of the Xiaokele area (after QIGE, 2018).

949 Permissions for this figure are not required from the original source(s)/copyright

950 holder(s) to publish. Coreldraw X8 was used to create the map.

951

952 Figure 3. Microscope photographs for syenogranite (a) and diabase (b) from the

953 Xiaokele area. Abbreviations: Pl = plagioclase; Cpx = clinopyroxene; Hb =

954 hornblende; Bt = Biotite; Qtz = Quartz; Kfs = alkali feldspar.

955

956 Figure 4. Cathode luminescence microphotographs of zircons for syenogranite and

957 diabase from the Xiaokele area.

958

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959 Figure 5. Zircon U–Pb concordia diagrams for syenogranite (a) and diabase (b) from

960 the Xiaokele area. The weighted mean ages and MSWD are shown in each figure.

961

962

963 Figure 6. (a) Plots of SiO2 vs. (Na2O + K2O) (after Irvine and Baragar, 1971), (b)

964 SiO2 vs. K2O (after Peccerillo and Taylor, 1976), and (c) A/CNK vs. A/NK (after

965 Maniar and Piccoli, 1989) for syenogranite and diabase from the Xiaokele area. Data

966 for the Late Devonian–Early Carboniferous igneous rocks of the Great Xing’an Range

967 and its adjacent regions are from Dai et al., 2012, Li et al., 2014a, Dong et al., 2016, 968 Zhao et al., 2016, and Feng et al.,Draft 2018b, data for the Late Carboniferous–Early 969 Permian igneous rocks of the Great Xing’an Range and its adjacent regions are from

970 Sui et al., 2009, Chen et al., 2014, Fan et al., 2014, Li et al., 2014a, Dong et al., 2016,

971 Li et al., 2017, Shi et al., 2019, Yang et al., 2019, and Ma et al., 2020.

972

973

974 Figure 7. Chondrite-normalized REE patterns (a, c) and primitive mantle-normalized

975 spider diagrams (b, d) for syenogranite and diabase from the Xiaokele area. The

976 chondrite values are from Boynton (1984), the primitive mantle and N-MORB values

977 are from Sun and McDonough (1989).

978

979

980 Figure 8. (a) Plots of zircon U–Pb ages vs. Hf(t) values for syenogranite and diabase

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981 from the Xiaokele area (Yang et al., 2006). (b) Close-up view of the distribution of

982 samples in Figure 8a. Abbreviations: CAOB–Central Asian Orogenic Belt; YFTB–

983 Yanshan Fold and Thrust Belt.

984

985 Figure 9. SiO2 vs. P2O5 (a), Rb vs. Th (b), 10000Ga/Al vs. Ce (c), 10000Ga/Al vs. Zr

986 (d), 10000Ga/Al vs. (Na2O + K2O) (e), (Zr + Nb + Ce + Y) vs. (Na2O + K2O)/CaO (f),

987 Th vs. Th/Nd (g), La vs. La/Sm (h), and La vs. La/Yb (i) diagrams for the Xiaokele

988 syenogranite. (a, b) after Chappell, 1999; (c–f) after Whalen et al., 1987; The domain

989 for highly fractionated I-type granites in NE China are from Wu et al., 2003; 990 FG = fractionated M-, I-, and S-typeDraft granites; OGT = unfractionated M-, I-, and 991 S-type granites.

992

993 Figure 10. Nb/Yb vs. Th/Yb (a), Th/Nb vs. Ba/Th (b), Th/Yb vs. Ba/La (c), and

994 La/Nb vs. La/Ba (d) diagrams of the Xiaokele diabase. (a) after Pearce, 2008, data for

995 primitive mafic melts derived from subduction-modified lithospheric and

996 asthenospheric mantle are from Leat et al., 2002; (b, c) after Hanyu et al., 2006; The

997 reference fields for OIB, MORB and high U/Pb mantle source (HIMU) in (d) are from

998 Saunders et al., 1992. CLM: Continental lithospheric mantle.

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