Zircon U-Pb Chronology, Geochemistry, and Petrogenesis of the High Nb-Ta Alkaline Rhyolites at the Tuohe Tree Farm, Northern Volcanic Belt, Great Xing’An Range, China

Canadian Journal of Earth Sciences

Zircon U-Pb Chronology, Geochemistry, and Petrogenesis of the High Nb-Ta Alkaline Rhyolites at the Tuohe Tree Farm, Northern Volcanic Belt, Great Xing’an Range, China

Journal: Canadian Journal of Earth Sciences

Manuscript ID cjes-2018-0332.R2

Manuscript Type: Article

Date Submitted by the 29-May-2019 Author:

Complete List of Authors: Sun, Guosheng; Jilin University Zhao, Tianxue; Jilin University, College of Earth Science Jin, Ruixiang; Jilin University Wang, Qinghai;Draft Jilin University Xingan Block, High Nb-Ta, Alkaline Rhyolite, Zircon U-Pb Chronology, Keyword: Geochemistry, Petrogenesis

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

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1 Zircon U-Pb Chronology, Geochemistry, and Petrogenesis of the High Nb-Ta

2 Alkaline Rhyolites at the Tuohe Tree Farm, Northern Volcanic Belt, Great Xing’an

3 Range, China

4 Guosheng Sun；Tianxue Zhao1；Ruixiang Jin；Qinghai Wang

5 College of Earth Science, Jilin University

6 Address of all authors: No.2199, Jianshe Street, Jilin University, Changchun, China

7 130061

Draft

1 Corresponding author (E-mail: [email protected]; Address: No.2199, Jianshe Street, Jilin University, China 130061; Fax: 0431-88502055; Tel: 15044096612) 1

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9 Abstract: We studied newly found high Nb-Ta alkaline rhyolites in the Northern

10 volcanic belt of the Great Xing’an Range, China. The LA-ICP-MS U-Pb weighted

11 mean age is 114.07±0.55 Ma, indicating that the rocks formed during the late Early

12 Cretaceous and were the product of the late eruption of a Mesozoic volcano. The

13 major element contents are characterized by high Si, rich K, low Fe, and poor Ca and

14 Mg. In the Total Alkaline–Silicon diagram, the sample points are in the alkaline

15 rhyolite region. Meanwhile, rare earth elements show obvious Ce/Ce* positive

16 anomalies and Eu/Eu* negative anomalies; in addition, trace elements are 17 characterized by high Nb, Ta, andDraft Yb and low Sr. The two stage Nd isotopic model

18 age T2DM of the depleted mantle is between 799–813 Ma, indicating that there

19 diagenetic material originated from the depleted mantle or partial melting of newly

20 formed young crustal materials. The source rocks melted at a relative shallow depth

21 (< 30 km), under lower pressure (< 0.5 Gpa) and high oxygen fugacity; moreover, the

22 residues in the source region were Ca-rich mafic plagioclase + amphibole +

23 orthopyroxene. In the Nb-Y-3Ga and Nb-Y-Ce diagrams, the sample points are in the

24 A1 type region. It can be concluded that the mantle-derived basaltic magma

25 underplated and supplied the heat sources for partial melting of the metamorphic

26 crustal rocks in an intraplate extensional tectonic environment related to a rift, mantle

27 plume, and hot spot.

28 KEYWORDS: Xingan Block, High Nb-Ta, Alkaline Rhyolite, Zircon U-Pb

29 Chronology, Geochemistry, Petrogenesis.

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30 Introduction

31 The Northern volcanic belt of the Great Xing’an Range is the superimposed part

32 of the ancient Asian oceanic tectonic domain, the Pacific domain, and the

33 Mongolia–Okhotsk oceanic domain（Wu et al. 2011; Xu et al. 2009; Zhou Jian-bo et

34 al. 2016). The area was subject to formation of the Xingan block metamorphic

35 basement during the Precambrian, closure of the paleo-Asian ocean and the

36 combination of several microcontinents during the Proterozoic (Zhang Xing-zhou et

37 al. 2006), and remote superposition and transformation caused by the closure of the

38 Mongolia–Okhotsk ocean and subduction of the paleo-Asian ocean plate (Ge 39 Wen-chun et al. 1999; Lin Qiang etDraft al. 1998; Ren Jisun et al. 1999; Shao Ji-an, Zhang 40 and Lu-qiao 1999; Wu et al. 2007; Zhao Guo-long et al. 1989). The area is widely

41 covered by Mesozoic mafic and felsic volcanic rocks. It is the largest Mesozoic

42 volcanic rock zone and an important metallogenetic belt of nonferrous metals as well

43 as rare and rare earth elements in China. Thus far, many controversies remain

44 regarding the dynamic background of the formation of the Great Xing’an Range

45 Mesozoic volcanic rock’s minerals and the nature of the magma source because of the

46 complex tectonic evolution and the superposition of multiple tectonic domains in the

47 study area (Chen Yan-jing et al. 2012; Fan et al. 2003; Ge Wen-chun et al. 1999; Lin

48 Qiang et al. 1998; Meng R 2003; Wang et al. 2007; Wu et al. 2011; Xu et al. 2009;

49 Zhang et al. 2008; Zhang et al. 2010; Zhao Yue et al. 1994). The origin of the

50 volcanic belt has been a high-profile issue and a focus of Chinese geologists.

51 During the 1:50,000 Mineral Geological Survey implemented over recent years,

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52 several widely distributed high Nb–Ta (alkaline) rhyolites were discovered in the

53 Great Xing’an Range, of which the Nb2O5 contents reach on average more than

54 0.03% with the highest content exceeding 0.06%. These values exceed the 0.02% of

55 industrial grade niobium tantalum ore deposits in China. The Nb and Ta contents in

56 the rhyolites are generally high and the rocks have not been superimposed or

57 reformed via later hydrothermal solutions. This shows that the Nb and Ta enrichment

58 was restricted by the nature of the source area and magmatic evolution. Recently, high

59 Nb-Ta alkaline rhyolite was discovered in the Baiyingaolao Formation in the northern

60 part of the Xingan block in the Great Xing’an Range. Many studies were completed 61 and are reported in this paper to provideDraft a constraint basis for the tectonic background 62 of the formation of the Great Xing’an Range volcanic rock belt and the nature of the

63 magmatic source through zircon U-Pb chronology and the geochemical characteristics

64 of the high Nb-Ta alkaline rhyolite.

65 Geological background and sample description

66 Geological background

67 The main volcanic belt in the Great Xing’an Range is west of the

68 Hegenshan–Heihe fault, east of the Xinlin–Xiguitu fault, and north of the

69 Xilamulun–Changchun paleo-Asian oceanic suture (Figure 1a), distributed in a NE

70 direction, the main part of which are the Great Xing’an Range w composed of

71 Mesozoic volcanic rocks. The Xingan block metamorphic basement is represented by

72 the Xinghua Ferry Group that formed from the Neoarchean to Proterozoic (Ge

73 Wen-chun et al. 2007; Şengör et al. 1993; Xu et al. 2009). It is composed of

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74 sillimanite-garnet bearing gneiss, felsic gneiss, amphibolite, graphite schist, and high

75 greenschist facies – high amphibolite facies metamorphic rocks (Chen Yan-jing et al.

76 2012; Zhao Yue et al. 1994). It underwent high-greenschist facies metamorphism and

77 high-breccia facies metamorphism (HBGMR, 1993). Proterozoic covers are mainly

78 distributed in the upper Heilongjiang depression in the northern Xingan block, but are

79 sporadically exposed in the western and south-central Xingan block;

80 Silurian–Devonian–early Carboniferous strata are continuously deposited marine

81 facies or shallow-marine facies and the late Carboniferous palaeogeographic pattern

82 includes continental sediments to the north and marine sediments to the south (Zhou 83 Jian-bo et al. 2016). The Jurassic rocksDraft in the Mesozoic – Cretaceous basic and acidic 84 lava and pyroclastic rocks are exposed widely in the Xingan block, including the

85 following groups from oldest to youngest: the Tamulangou (J2tm), Manketouebo

86 (J3mk), Manitu (J3mn), Baiyingaolao (K1b). and Meiletu groups (K1ml) according to

87 the lithology and eruption age. The Tamanguou Formation (J2tm) is the lowest part of

88 the Mesozoic Daxing 'anling volcanic belt of Middle Jurassic age. Its lithology is

89 mafic-intermediate volcanic rocks with normal sedimentary rocks. The Manketou

90 Obo formation (J3mk) is discordant from the Tamangou Formation (J2tm) of early

91 Late Jurassic age and its lithology is mainly acid volcanic lava and acidic volcanic

92 clastic lava. The Manitou Formation concordantly overlies the Manketou Obo

93 Formation (J3mk) of late Late Jurassic age. Its lithology is neutral (dacitic – andesitic)

94 volcanic lava and volcanic clastic lava. The Baiyingaolao Formation disconcordantly

95 overlies the Manitu Formation of early Early Cretaceous age. Its lithology is acidic

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96 lavas and acidic volcanic clastic lava with normal sedimentary rocks. The Meiletu

97 Formation (K1ml) disconcordantly overlies the Baiyingaolao Formation. It is mainly

98 composed of a set of intermediate-basic volcanic rocks, including fumarolic

99 amygdaloid or dense massive trachy andesite, basalt, etc. (Regional geology of Inner

100 Mongolia, 1991. According to lithologic characteristics and zircon U-Pb dating, the

101 high Nb-Ta alkaline rhyolite studied in this paper was found in early Cretaceous

102 stratum of the Baiyingaolao Formation in the northern part of the Xingan block; it is

103 the upper effusive facies lithologic member (Figure 1b).

104 Sample description 105 The high Nb-Ta alkaline rhyolitesDraft are exposed in the western Tuohe Tree Farm in 106 the Kyihe county of the Oroqen Autonomous Banner. East longitude 122°34′20″,

107 north latitude 50 ° 18 ′ 28 ″ .The rhyolites are belt-like and distributed in a NNW

108 direction in an area of 3 km2. They form a parallel unconformable contact with the

109 underlying late Jurassic andesite of the Manitu group to the west and south, cover the

110 early Cretaceous rhyolitic debris-crystal tuff of the Baiyingaolao Formation to the

111 north, and are covered by Quaternary rocks to the east (Figure 1).

112 The fresh surface of the alkaline rhyolite is grayish purple or gray white with

113 porphyritic, rhyolitic, and massive structure (Figure 2). Approximately 8% of the rock

114 is phenocrysts composed of sanidine, quartz, and minor biotite. The sanidine shows

115 euhedral-subhedral plating with micro cracks developed, mostly showing a

116 porphyritic or glomero-porphyritic texture, and biaxial crystals (2V = 63°). It is a type

117 of high temperature sanidine with a weak stripe structure visible and Cartesian double

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118 crystal or Manebach twins locally containing oligoclase; the diameter of the sanidine

119 is 1–2 mm and the content is 5%. The quartz shows xenomorphic granulation and a

120 diameter of 0.5–1 mm; its content is approximately 3%.

121 Biotite, pyrochlore, and ilmenite – magnetite occasionally occur in the alkaline

122 rhyolite. Biotite is flaky, brown, palm red and reddish brown; some biotite minerals

123 have darkened edges. The biotite shows parallel extinction, a group of perfect

124 cleavage, and is 0.1–0.5 mm in particle size. The pyrochlore is dark brown and

125 reddish brown, extremely convex, irregularly granular, and 0.1–0.5 mm in particle

126 size. The Nb - Ta mainly occurs in the pyrochlore (Fig. 2c) and titanomagnetite (Fig.

127 2d). Electron probe test results showDraft that the Nb2O5 content in the titanomagnetite 128 reaches 1.89%–2.28%. The matrix has a coarse-to-fine structure, a micro-embedded

129 crystal-containing structure, and a particle structure. Alkali feldspar microcrystals,

130 quartz, and dusty ilmenite are arranged in a semi-parallel arrangement.

131 Sample analysis methods

132 Analyses of major and trace elements were completed at the Jilin University Test

133 Center. The determination of major elements was as follows: first, we chose seven

134 fresh rock samples; second, we crushed them to less than 200 mesh using an agate

135 mortar; third, samples were melted into glass cake; finally, we determined major

136 elements using an XRF-1500X fluorescence spectrometer with an analytical precision

137 of approximately 1%. However, the determination of trace elements was as follows:

138 first, we weighed 40 mg samples and placed them into a Teflon tank; second, we

139 added HF and HNO3 and thoroughly dissolved them; third, we diluted the sample

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140 with 1% HNO3; finally, we determined the trace and rare earth elements using the

141 dual focus inductively coupled plasma mass spectrometer (ICP-MS) ELEMENT

142 produced by Finnigan-MAT company with an analytical precision greater than 5%.

143 The zircon particles in good crystal form and standard samples for dating were

144 separated using the conventional gravity and magnetic separation method and selected

145 using a binocular microscope. Then, they were immediately placed into a colorless

146 and transparent epoxy resin and turned into targets after solidification. Then, the

147 targets were polished until the central part of the zircon was exposed. The zircon

148 sample in good crystal form was chosen for cathodoluminescence (CL) photography 149 using the Mono CL3+ CathodoluminescenceDraft System produced by British Gatan 150 company. CL photography was completed at the Laboratory of Tianjin Institute of

151 Geology and Mineral Resources. Laser Ablation Inductively Coupled Plasma Mass

152 Spectrometry (LA-ICP-MS) zircon dating was completed at the Laser Plasma Mass

153 Spectrometry Laboratory at the China University of Geosciences (Beijing campus)

154 using the laser plasma mass spectrometer that was a combination of the 193=nm laser

155 denudation injection system (UP 193SS) produced by the American New Wave

156 company and the Aglient7500a type four-stage bar plasma mass spectrometer

157 produced by the American AGILENT Technology Co., Ltd. During the experiment,

158 the laser working frequency was 10 Hz; the beam diameter of the test point was 30

159 μm; the pre-ablation time was 5 s; the ablation time was 45 s; and high purity He gas

160 denudation material was used as the carrier gas stream (the flow rate was 0.88 L/min)

161 The isotopic ratio was used to normalize based on the standard zircon 91500 as the

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162 external standard. The blind samples included standard zircon TEMORA and Qinghu.

163 The age was calculated via the international standard program Isoplot. The zircon

164 U-Pb isotopic ratio was determined using ICP-MS and calculated via the Glitter

165 program. The elemental content in the zircon was determined based on the

166 international standard NIST610 which acted as the external standard and Si which

167 acted as the internal standard; the blind samples included NIST612 and NIST614. The

168 error of every single data point was 1σ, the weighted mean value error was 2σ, and

169 the average age was calculated using the 206Pb/238U age.

170 The Sr and Nd isotopic tests were completed at the laboratory of the Tianjin 171 Institute of Geology and Mineral Resources.Draft The samples were dissolved using mixed

172 acid (HF+HClO4) and attacked for more than 12 h under high-temperature conditions

173 in a closed Teflon dissolving device. Then, Sr, the output of the Isotope Concentration

174 (IC) process, was purified a second time. The purification of Nd was supported by the

175 Di-(2-ethylhexyl)phosphoric acid (HDEHP) color layer technology. The content and

176 isotopic ratio were all determined using Triton thermo-ionization mass spectrometry.

177 The level of the system blank of the whole process was stable at the following values:

178 Rb = 5.6×10-10 g, Sr = 3.8×10-10 g, Sm = 3.0×10-11 g, Nd = 5.4×10-11 g. During the

179 sample testing, the Nd-Sr isotopic ratios of the BCR-1 Nd standard samples and

180 NBS-607 Sr standard samples were as follows: 143Nd/144Nd = 0.512739±5 (±2σ)

181 and87Sr /86Sr = 1.200050±5 (±2σ), respectively. The Sr and Nd isotopic test data were

182 exponentially processed with mass fractionation correction in which the internal

183 standards are as follows: 88Sr /86Sr = 8.37521 and 146Nd/144Nd = 0.7219.

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184 Results

185 Zircon U-Pb dating and trace element characteristics

186 Twenty-nine zircon samples were selected from the alkaline rhyolite for LA-ICP-

187 MS U-Pb dating. The samples appeared pink brown, showing a

188 hypidiomorphic-euhedral short column texture, and the crystal form was mainly a

189 combination form composed of {100}+{110}+{111} and

190 {110}+{110}+{311}+{131}. The particle sizes were mostly between 0.1 and 0.25

191 mm, with a ratio of length to width between 1:1 and 3:1. It can be seen from the CL

192 photo (Figure 3) that the zircon show an oscillatory zoned structure of magmatic 193 origin whose Th/U ratio was betweenDraft 1.1 and 2.2 (Table 2). It also shows the typical 194 characteristics of magmatic crystallized zircon (Belousova et al. 2002; Koschek

195 1993). Zircon has a high rare earth element content and the total amount of rare earth

196 elements (∑REE) was 1912–3399 µg/g. The ratio of LR/HR was 0.09–0.21, implying

197 significant REE fractionation. In the chondrite-normalized partition diagram of rare

198 earth elements, the samples are inclining to left (Figure 4a), implying a significant

199 enrichment in heavy rare earth elements (HREEs). There are obvious Ce/Ce*

200 (Ce/Ce*=9-384) positive anomalies and Eu/Eu* (Eu/Eu*=0.26–0.29) negative

201 anomalies, consistent with the characteristics of REEs in crustal source magmatic

202 zircons (Hoskin and Schaltegger 2003). Strong Ce/Ce* positive anomalies suggest

203 that the high Nb-Ta alkaline rhyolite formed under an environment of higher oxygen

204 fugacity(Burnham and Berry 2012; Mass et al. 1992); the element Eu should occur

205 as Eu3+ when the magma has high oxygen fugacity and cannot be fractionated from

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206 other trivalent rare earth elements; thus, the Eu/Eu* negative anomaly is the

207 inheritance of the low Eu content in the magma. The zircon 206Pb/238U ages of 29

208 sample points are between 111 and 116 Ma (Table 2); in zircon U-Pb dating

209 harmonious graphs (Figure 4b), the data points are centrally distributed and on or

210 near the harmonious line. A weighted average 206Pb/238U age of 114.07±0.55 Ma

211 (MSWD = 0.63, n = 29) (Table 2, Figure 4b) shows that the eruption age of the

212 rhyolite is late Early Cretaceous.

213 Characteristics of major and trace elements

214 Major elements 215 The major element contents inDraft the high Nb-Ta alkaline rhyolite are characterized

216 by high Si, rich K, low Fe, and poor Ca and Mg. The SiO2 content in the rock is

217 between 72.35% and 73.22%, indicating that the rock is acidic; moreover, the Al2O3

218 content is 13.18%–13.60% and the aluminum saturation index A/CNK is 0.88–1.05,

219 indicating that the rock is quasi-aluminous. Total alkali (K2O+Na2O) content varies

220 between 9.39% and 11.43%, showing that the rock is obviously alkaline rich. The

221 K2O/Na2O ratio is 1.03–2.16 with an average of 1.52, implying that the rhyolite is

222 potassic; the FeOT contents (1.53%–2.35%) are low while the CaO (0.12%–0.18%),

223 TiO2 (0.19%), and MgO contents (0.04%–0.08%) are lower. In the SiO2-Na2O+K2O

224 silicon-alkali diagram (Figure 5a), the rhyolite samples are above the

225 alkaline-subalkaline boundary in the rhyolite region, indicating that are alkaline

226 rhyolite. In the discrimination diagram of A/CNK-A/NK aluminum saturation (Figure

227 5b), the sample points are in the peralkaline region, and in the SiO2- K2O diagram

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228 (Figure 5c), the sample points are in the shoshonite series region. There is standard

229 mineral quartz in the CIPW standard minerals calculations (22.56%–23.93%),

230 showing that the rock is silicon saturated or oversaturated. The K-feldspar contents

231 (Or) (32.72–46.35) and albite (Ab) (24.75–37.87) in the standard minerals are high

232 and anorthite (An) was not found, consistent with the characteristics of rich alkalinity

233 and poor Ca. Acmite (Ac) (2.92–3.15) and sodium silicate (Ns) (0.29–1.08) occurs,

234 but no alkaline minerals such as alkaline pyroxene or alkaline amphibole are found.

235 Trace elements

236 The total REE content in the rock (ΣREE) is high, from 86.87×10-6 to 161.72×10-6

237 (Table 3, Figure 6a). The LREE/HREEDraft ratio is 3.40–6.87 and the LaN/YbN ratio is 238 3.76–4.54; thus, there was moderate fractionation between LREE and HREE. The

239 ratios of LaN/SmN are 2.87–5.85; thus, there was significant LREE fractionation. The

240 total HREE content is high, 10 times higher than that of the standard chondrite; the

241 ratios of GdN/YbN (0.54–0.80) suggest the enrichment of HREEs and weak

242 fractionation (Figure 6a). The Sr/Y ratio (0.04–0.35) was also low, indicating that a

243 large number of garnet minerals that were primarily stable under the high-pressure

244 condition in the magma source area melted during a later period The diagenetic

245 pressure is low while the depth is very shallow (Evans and Hanson 1993; Hanson

246 1978); YbN (23.76) > HoN (21.95), showing a slight loss in medium rare earth

247 elements (MREEs) and suggesting that there was residual amphibole in the source

248 area. The Ce/Ce* ratio is between 1.05–1.31, a positive anomaly, indicating that the

249 rocks formed in a strong oxidizing environment or there was an inheritance of high Ce

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250 minerals in the source area. The strongly depleted Eu/Eu* ratio (0.39–0.44) and low

251 Ca content in the major elements imply that basic plagioclase rich in Ca was the main

252 residual in the source area.

253 It can be seen from the trace element spider diagrams (Figure 6b) that Rb, Nb, Ta,

254 Zr, Hf, Th, and U are quite enriched in the rocks, but Ba, Sr, P, and Ti are obviously

255 depleted. NbN and TaN, the primitive mantle standardization value of Nb and Ta in the

256 rocks, is 153.04–177.70 and 143.75–343.0, respectively, suggesting obvious

257 enrichment of Nb and Ta and indicating that the rocks are high Nb-Ta alkaline

258 rhyolites. The Nb2O5 + Ta2O5 content ranges from 0.026% to 0.031%, reaching and 259 exceeding the industrial grade of 0.02%Draft of niobium tantalum ore in China. The Nb/Ta 260 ratio of the rock is 7.2–14.9, lower than that of the primitive mantle (Nb/Ta=17.5)

261 (Jochum et al. 1997; Mc Donough and Sun 1995; Sun and Mc Donough 1989) and

262 falling in the Nb/Ta ratio range of continental crust (Nb/Ta=10–14). The Zr and Hf

263 contents in the rhyolite are high, among which, the Zr content is as high as 447.9×10-6

264 – 543.7×10-6, suggesting that zirconium-rich minerals such as zircon were

265 concentrated and melted in the source region. The contents of basic compatible

266 components such as Co (0.18×10-6–0.24×10-6), Ni (0.01×10-6–0.77×10-6), and Cr

267 (0.07×10-6–0.41×10-6) are low; the Sr content in the rock is 1.86×10-6–8.8×10-6, <

268 100×10-6, and the Yb content is 3.35×10-6 – 4.65×10-6, > 2×10-6, suggesting that the

269 rock is an 'extremely low Sr and high Yb' type (Zhang Qi et al. 2006) rhyolite. The

270 low Sr also suggests that there was plagioclase residual in the source area while the

271 high Yb implies that garnet is a molten phase in the source region. The Rb/Sr ratios

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272 (27.05–135.23>10) and Th/U ratios (4.57–7.77) of the rocks are all high, implying

273 that the source rocks of the alkaline rhyolite were continental crust materials.

274 Characteristics of Sr and Nd isotopes

275 We completed tests and analyses of the compositions of the Sr and Nd isotopes of

276 the four alkaline rhyolite samples in the study (Table 4). The results are as follows:

277 the ratio of Rb/Sr is 199.72–208.95 while the ratio of Sm/Nd is 0.12–0.16, indicating

278 that the alkaline rhyolite is characterized by high Rb/Sr and low Sm/Nd. ISr, the initial

279 ratio of the Sr isotope, is 0.70437–0.72621, while the εSr(t) value is -0.01–310.6.

280 Moreover, the ISr and εSr(t) values of the four samples vary greatly; among the four

281 samples, the εSr(t) values of three Draftsamples are all positive but one is negative. The ISr 282 values of one sample are 0.7040–0.7060 while those of the other three samples are far

143 144 283 greater than 0.7060. INd, the initial ratio of Nd/ Nd, is 0.512553–0.512590 and the

284 εNd(t) values are positive (1.2–1.9), the same as those of the continental crust derived

285 granite in the Xingmeng orogenic belt (Mass et al. 1992; Shao and Zhang 1999). The

286 characteristics of the Sr and Nd isotopes indicate that there was not only

287 mantle-derived materials but also crustal materials in the magmatic source area. The

288 two-stage Nd isotopic model age T2DM of the depleted mantle is between 799 and 813

289 Ma, similar to the model age of the granites in the Center Asia Orogenic Belt which is

290 dominantly between 600–800 Ma (Guo Zhi-jun et al. 2014; Hong Da-wei et al. 2000;

291 Zhao Zhen-hua et al. 2008). The T2DM value is much greater than the formation age of

292 the high Nb-Ta alkaline rhyolite, showing that the formation of the rocks is related to

293 partial melting of crustal materials. In a word, the source rocks of the high Nb-Ta

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294 alkaline rhyolite were crust composed of mantle materials, basalt, and sedimentary

295 clastic rocks.

296 Discussion

297 Diagenetic age, petrogenesis type, and tectonic setting

298 Diagenetic age

299 The Mesozoic volcanic rocks of the Great Xing’an Range include the Tamulangou

300 (J2tm), Manketouebo (J3mk), Manitu (J3mn), Baiyingaolao (K1b) and Meiletu groups

301 (K1ml) from oldest to youngest (GMBIM, 1996), formed during the period 122–173

302 Ma (Chen Zhi-guang et al. 2009; Meng En et al. 2011; Xu Mei-Jun et al. 2011; Xu 303 Wen-liang et al. 2008; Zhang Ji-hengDraft 2009; Zhang et al. 2010; Zhang et al. 2008). 304 The volcanic eruptions can be divided into three stages: early Late Jurassic (159–162

305 Ma), early Early Cretaceous (141–139 Ma), and late Early Cretaceous (123–127

306 Ma)(Gou Jun et al. 2010; Wang Jian-guo et al. 2013). "Regional Geological

307 Chronicles of the Inner Mongolia Autonomous Region" (1993（IMBGMR, 1991）and

308 "Lithostratigraphy of the Inner Mongolia Autonomous Region" (1996) (GMBIM,

309 1996) determined the formation age of the rocks in the Baiyingaolao Formation to be

310 Late Jurassic because detailed high-precision chronological data were not available at

311 that time. During recent years, zircon LA-ICP-MS U-Pb chronology study of the

312 Baiyingaolao Formation indicated that the formation age of the volcanic rocks in the

313 Baiyingaolao Formation is 125–144 Ma (Gou Jun et al. 2010; Huang Ming-da et al.

314 2016; Nie Li-jun et al. 2015; Si Qiu-liang et al. 2015; Wang Jian-guo et al. 2013;

315 Zhang Le-tong et al. 2015; Zhang Xiang-xin et al. 2016; Zhang Xue-bin et al. 2015),

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316 i.e. the Early Cretaceous. The high Nb-Ta alkaline rhyolite of the studied Tuohe Tree

317 Farm is in parallel unconformable contact with the underlying Late Jurassic rocks of

318 the Manitu group, covering the rhyolitic debris–crystal tuff and continuous sediments

319 of the upper part of the Baiyingaolao Formation. The magmatic zircon U-Pb age of

320 the rhyolite is 114.07±0.55 Ma, showing that the formation age of the alkaline

321 rhyolite is late Early Cretaceous. Compared to the formation age of the Baiyingaolao

322 Formation volcanic rocks in the Great Xing’an Range in previous studies (>122 Ma),

323 the alkaline rhyolite formed later (114 Ma) and was the product of late volcanic

324 eruptions of the volcanic rock belt in the Great Xing’an Range. 325 Petrogenetic type and tectonic settingDraft 326 Some researchers believe that after suturing of the north China plate and the

327 Siberian craton along the Xilamulun–Changchun suture from the late Late Permian to

328 early Early Triassic (Li Jin-yi et al. 2007; Liu Jian-feng et al. 2016; Wang Cheng-wen

329 et al. 2008), the Great Xing’an Range region had completed the transformation from

330 the paleo-Asian oceanic domain to the superposition of the circum-Pacific tectonic

331 domain and the Mongolia–Okhotsk oceanic tectonic domain during the

332 Mesozoic–Cenozoic (Ge Wen-chun et al. 1999; Lin Qiang et al. 1998; Ren Jisun et al.

333 1999; Shao Ji-an et al. 1999; Wu et al. 2007; Zhao Guo-long et al. 1989). However,

334 until now, direct evidence of subduction of the paleo-Pacific plate along the eastern

335 margin of the Eurasian plate during the early and middle Mesozoic has not been found

336 in eastern China and East Asia (Sao Ji-an et al. 2001). Zhao et al. (1994) and Xu et al.

337 (2013) suggested that it was mainly the Songliao Basin and its eastern region in

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338 Northeast Asia that were influenced by the Mesozoic circum–Pacific tectonic system,

339 while the western Songliao Basin such as the Xingan block and the north margin of

340 north China were mainly influenced by the Mongolia–Okhotsk oceanic tectonic

341 system. However, many controversies remain regarding the subduction direction and

342 closure time of the Mongolia–Okhotsk ocean (Chen Zhi-guang et al. 2010; Huang

343 Ming-da et al. 2016; Jiang Si-hong et al. 2010; Li Jin-yi et al. 2007;Liu Jian-feng et al.

344 2016; Nie Li-jun et al. 2015; Sao Ji-an et al. 2001; Wang Cheng-wen et al. 2008; Xu

345 Wen-liang et al. 2013; Zeng Wei-shun et al. 2014; Zhang Xiang-xin et al. 2016).

346 Some researchers believe that both the formation of the Triassic porphyry Cu-Mo 347 deposits in the Ergun block and Draft the formation of the Triassic granite in the north 348 segment of the Ergun block are related to the subduction of the Mongolia–Okhotsk

349 ocean to the south (Chen Zhi-guang et al. 2010; Jiang Si-hong et al. 2010; Wu et al.

350 2011; Zeng Wei-shun et al. 2014) and have speculated that the Mongolia–Okhotsk

351 ocean was closed during the Triassic (Jiang Si-hong et al. 2010) while others

352 suggested during the late Jurassic–early Cretaceous (Cogné M et al. 2005;

353 Kravchinsky et al. 2002; Metelkin et al. 2010; Parfenov et al. 2001; Pei et al. 2011;

354 Zonenshain et al. 1990).

355 Major elements of the high Nb-Ta alkaline rhyolite in the Tuohe Tree Farm are

356 characterized by rich Si and K and poor Ca and Mg while trace elements are quite

357 enriched in Rb, Th, Nb, Ta, Zr, Hf, Ga, and Y but depleted in Sr, Ba, Ti. and P. The

358 chondrite-normalized partition curve of the REEs varies as a 'V' type with obvious Eu

359 negative anomalies, with the same typical chemical composition as an A-type granite

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360 (Collins et al. 1982; Ge Wen-chun et al. 2005; Zhang Qi et al. 2012; Zhao Zheng-hua

361 et al. 1997). In the tectonic environment discriminated diagrams(Figure 7a,b,c), the

362 rock samples are in the intraplate granite region, indicating that the alkaline rhyolite

363 was formed in an intraplate extensional tectonic environment.The 10,000 Ga/Al ratio

364 is between 3.81–4.04, higher than the lower limit ratio of an A-type granite(i.e. 2.6).

365 In the rhyolite genesis discrimination diagram of 10,000 Ga/Al (Figure 8a, b, c, d), the

366 rock samples are all in the A-type granite region. In the Nb-Y-3Ga and Nb-Y-Ce

367 diagrams for discrimination of A1 and A2 tectonic settings (Eby 1992; Whalen et al.

368 1987), the sample points are all in the A1=type region (Figure 8e, f), indicating that 369 the alkaline rhyolite formed inDraft an intraplate extensional and not in a tensional 370 tectonic environment developed by post-collisional or post-orogenic continental crust

371 collapse. The eruption of the 'extremely low Sr, high Yb' A1 type alkaline rhyolite

372 implies that the Xingan block was in an intraplate non-orogenic period during the late

373 Early Cretaceous (114 Ma), indicating that the Mongolia–Okhotsk ocean closed

374 before the early Cretaceous. Based on this, it is speculated that the closing time of the

375 Mongolia–Okhotsk Ocean occurred during the Late Jurassic.

376 Nature of the magmatic source

377 The A-type granite formed under alkali rich, anhydrous, and non-orogenic

378 conditions (Loiselle M C and Wones D, 1979; Zhang Qi et al. 2012). The anhydrous,

379 high-viscosity A-type granitic magma and a small density difference between the

380 rock-forming minerals and granitic magma was not able to support large-scale

381 crystallization differentiation (Reid J B J et al. 1993; Zhang Qi et al. 1993); moreover,

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382 cumulates associated with the high Nb-Ta alkaline rhyolite and the synchronous

383 intermediate–basic igneous rocks were not found in the study area, indicating that the

384 rock was not formed via crystallization fractionation of mantle-derived magma. In the

385 La/Sm–La diagram (Figure 9a) to discriminate the magmatic process, the sample

386 points are distributed along the oblique line, showing that the diagenetic process was a

387 type of partial melting. Major elements in the rock are characterized by rich Si and K

388 and poor Ca and Mg while trace elements are quite enriched in Rb, Th, U, K, and Pb

389 but depleted in Ba, Sr, P, Ti, Co, Ni, and Cr The rock shows a Ce positive anomaly

390 and the εSr(t) value is between -18.21 and 102.94 All of these characteristics show 391 that the source rocks were alumina-richDraft ancient crust or originated from basic upper 392 crust (King et al. 1997; Wang Jian-guo et al. 2013). It is generally accepted that

393 aluminous A-type granite should form via partial melting of lower crust rich in Al

394 (Patino Douce 1997; Rajesh 2000), which is seemingly not consistent with the

395 geochemical characteristics of low Al content in alkaline rhyolite. However,

396 quasi-aluminous A-type granite can form via partial melting of lower crust rich in Al

397 because of the formation condition of alkaline A-type granite and the residues of the

398 Al-rich minerals in the source area. The residual phases of a partial melting

399 experiment on the A-type granite were mainly basic plagioclase rich in Ca +

400 orthopyroxene (Litvinovsky et al. 2000; Patino Douce 1997; Skjerlie and Johnston

401 1992; Turner Sand Rushmer T, 2010); this and the depletion of in the rock suggests

402 that there was residual amphibole in the source area. Ca-rich basic plagioclase and

403 amphibole are minerals rich in Al whose large-scale residues in the source area

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404 caused Al depletion in the magmatic lava and the formation of low-Al

405 quasi-aluminous A-type granite. Therefore, the source rock did not exclude the

406 Al-rich ancient crust.

407 Among the main characteristics of the alkaline rhyolite in the Tuohe Tree Farm is

408 the enrichment of Nb and Ta. In general, Nb and Ta mainly occur in Ca and Ti

409 minerals, such as rutile, sphene, perovskite, titanium (magnetic) iron ore, and allanite,

410 and secondarily exist in Fe and Mg minerals, such as pyroxene, amphibole and biotite

411 (Hong Da-wei et al. 2000). Because the rhyolite is poor in Ca, Ti, Fe, and Mg, the

412 source of Nb-Ta should be independent of Ca, Ti, Fe, and Mg minerals. The Nb 413 contents in the rocks increase as theDraft lithology changes from basic rock to acidic rock 414 and to alkaline rock, and among those rocks, the Ta content in acidic rock is the

415 highest; thus. it is difficult to explain why the Nb contents (99.57×10-6–85.7×10-6) and

416 Ta (5.75×10-6–13.72×10-6) are high in the alkaline rhyolite suing the reason of partial

417 melting of the volcanic rock. However, during the process of rock weathering, Nb, Ta,

418 and Zr tend to be enriched in hydrolytic sediments and terrigenous Nb, Ta, and Zr

419 placer can also form on river beds and coastlines. According to statistics,

420 approximately 24% of the world's Nb and Ta production originates from placer

421 deposits (Mou Bao-lei, 1999). It is speculated that continental or terrigenous

422 meta-sandstone or mudstone rich in Nb and Ta occurred in the Al-rich ancient crust.

423 Ce/Ce* positive anomalies in rock imply that the source rocks might be

424 terrigenous meta-sandstone or mudstone, not crustal or marine sediments. Volcanic

425 rocks typically show a Ce zero anomaly or weak negative anomalies. In marine

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426 sediments, sediments in the middle ridge regions of the ocean (Ce/Ce*=0.29) and in

427 basin areas (Ce/Ce*=0.55) show negative anomalies medium or above, except that the

428 oceanic ferromanganese crusts (nuclei) of colloidal genesis show an obvious Ce/Ce*

429 positive anomaly. The continental margins show Ce weak negative anomalies or

430 positive anomalies (0.90–1.30) (Murry et al. 1990; Zhao Zheng-hua and Zhou ling-li,

431 1997), indicating that Ce was relatively enriched in the continental or terrigenous

432 sediments. The rock is characterized by low Fe and Mn, showing that the Ce/Ce*

433 positive anomaly is not related to oceanic ferromanganese crusts (nuclei) and also

434 implying that the source rocks were not subducted oceanic crust but related to 435 terrigenous sediments. The Zr contentDraft (447.9×10-6–543.7×10-6) in the rocks is high, 436 implying that Zr and other Zr-rich minerals are enriched and melted in the source

437 region. The trace element analytical data (Table 1) show that the Ce content in the

438 zircon is relatively high and there are obvious positive Ce anomalies. To some extent,

439 the Ce positive anomaly in the rhyolite is an inheritance of the Ce positive anomaly in

T T 440 the zircon. In the SiO2-(FeO +MgO+TiO2) / FeO +MgO+TiO2 melting test diagram

441 to distinguish the nature of the source area (Patino Douce AE, 1999) (Figure 9b), the

442 sample points are at the intersection of the argillaceous rock trend line and basalt

443 trend line.

444 In addition, basic crustal materials are also involved in the magmatic source; INd,

445 the initial ratio of 143Nd/144Nd,is 0.512537–0.512539 and the εNd （ t ） value is

446 positive (1.9–2.0), while the εSr(t) value of a sample is -0.01. All of these results

447 imply that the source rock is from melting of basalt, a basic lower crust material

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448 derived from the mantle. Therefore, the source rocks of the high Nb-Ta alkaline

449 rhyolite should have originated from a magmatic source composed of Al-rich crustal

450 materials, basic crustal materials, and basalt. The two-stage Nd isotopic model age

451 T2DM of the depleted mantle is between 754–813 Ma, consistent with the

452 Neoproterozoic magmatic-thermal event of the Xingan block basement and the

453 formation age of the Khondalite in the Xingan block (Zeng Wei-shun et al. 2014;

454 Zhou Jian-bo et al. 2016). The Al-rich schist – gneisses and amphibolites of the

455 Xinghua ferry group in the Xingan block metamorphic basement are metamorphic

456 crustal rock (HBGMR, 1993; Wu et al. 2012; Zhou Jian-bo et al. 2016; Zhou et al. 457 2011a) whose formation age is betweenDraft 660–970 Ma (Miao Lai-cheng et al. 2003; 458 Zhou and Wilde 2013: Zhou et al. 2011b). Geochemical characteristics show that the

459 chemical composition characteristics of rare earth elements (Figure 10a) and trace

460 elements (Figure 10b) are similar to rhyolite. The chemical composition

461 characteristics and variation trend of the Al_rich schist_gneiss are closer to the

462 rhyolite(Figure10). The source rocks of the Al-rich schist–gneisses were mudstone

463 and sandstone, with Eu negative anomalies (δEu = 0.32–0.79) and Ce/Ce* positive

464 anomalies (0.90–1.30), indicating that the sedimentary environment of the Al rich

465 schist– gneisses was a metastable continental margin sedimentary environment. In

466 addition, the source rock of the amphibolites was weakly alkaline basalt (Dong Ce

467 and Zhou Jian-bo, 2012; Zhou Jian-bo et al. 2016). The metamorphic crustal rocks are

468 typical volcano sedimentary formations including sedimentary rocks composed of

469 metamorphic basic volcanic rocks and metamorphic terrigenous clastic rocks (Biao

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470 Shang-hu et al. 1999; Liu Xiao-guang, 2007; Sun Guang-rui et al. 2002; Wei-wei et al.

471 2016). The metamorphic crustal rocks composed of low alkaline basalt and

472 terrigenous clastic rocks in the Neoproterozoic Xinghua ferry group show

473 characteristics of mantle and crust material origin and their formation age and

474 geochemical characteristics are in accordance with those of the source rocks of the

475 high Nb-Ta alkaline rhyolite.

476 Physico-chemical conditions of the source area

477 The zircon saturation temperature of granitic magma can be calculated from the Zr

478 content and major elements in the rock by means of the following formula:

479 TZr=12900/[2.95+0.85M+ln(496000/ZrDraftmelt)] (Watson E B and Harrison T M ,1983), in 480 which 'T' is the absolute temperature, 'M' is the number of moles of

481 (Na+K+2Ca)/(Al×Si); Si+Al+Fe+Mg+Ca+Na+K+P = 1 (mole fraction) in the

482 calculation; and Zrmelt is the Zr content in the magma. The aforementioned formula

483 was used to calculate the zircon saturation temperature of six samples, which was

484 866℃–924℃ with an average of 881℃. The zircon saturation temperature can be a

485 good estimation of the magmatic emplacement temperature because zircon begins to

486 crystallize during the beginning of magma evolution and consequently the zircon

487 saturation temperature is near the magmatic liquidus. In addition, the zircon saturation

488 temperature can be approximated as the temperature of magma formation given the

489 approximate adiabatic rising and emplacement of granitic magma.

490 The poor Al, Ca, and Sr of the rock, and strong Eu/Eu* negative anomalies,

491 indicate that the residual phase of the magmatic source was plagioclase; the stability

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492 of plagioclase in the source area mainly depended on the pressure (Martin H et al.

493 2005), which was lower than 0.8 Gpa. The residue phase of basalt melting is

494 plagioclase + amphibole ± orthopyroxene ± ilmenite (no garnet)(Wu et al. 2002);

495 However, for the high Nb - Ta alkaline rhyolite in Tuohe Tree Farm, the pressure

496 under which the ‘very low Sr, high Yb’ A-type granitic magma formed might have

497 been much lower (<0.5 Gpa) (Zhang Qi et al. 2006). It is generally accepted that

498 A-type granite is low-oxygen-fugacity granite (Martin 2006; Reid et al. 1993; Wang

499 Yang et al. 2013); however, Anderson J L et al. (2005) and Dall' Agnol R et al. (2007)

500 argued that A-type granite can be completely formed under a condition of oxidation. 501 Obvious Ce/Ce* positive anomaliesDraft of zircon and rock indicate that the high Nb-Ta 502 alkaline rhyolite formed under a high-oxygen-fugacity condition. The alkaline

503 rhyolite at the Tuohe Tree Farm formed under conditions of low pressure (< 0.5 Gpa),

504 high temperature (>881℃), and high oxygen fugacity. It is speculated that the magma

505 source of the rhyolite was upper crust, a 'high level magma' formed from the melting

506 of upper crust.

507 Conclusion

508 (1) The weighted average of the zircon 206 Pb / 238 U age is 114.07 ±0.55 Ma,

509 indicating that rhyolites in the Tuohe Tree Farm formed during the end of Mesozoic

510 volcanic eruptions in the Great Xing’an Range, China.

511 (2) The major elements of rocks are rich in alkali and the trace elements are high in

512 Nb-Ta, low in Sr and high in Yb. Thus, the rhyolite in the Tuohe Tree Farm is

513 alkaline rhyolite with 'extremely low Sr, high Yb' and high Nb-Ta.

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514 (3) It is speculated from the petrochemical and Sr and Nd isotopic compositions, that

515 the magmatic source rock is metamorphic crust rock of the Xinghua ferry group in the

516 Xingan block metamorphic basement; the magma formation process was

517 characterized by the physical and chemical conditions of low pressure, high

518 temperature, and high oxygen fugacity.

519 (4) The magma formed following closure of the Mongolia–Okhotsk ocean in an

520 intraplate extensional tectonic environment related to a rift, mantle plume, and hot

521 spot, as the basaltic magma underplating supplied a heat source resulting in partial

522 melting of the metamorphic crustal rock of the Xinghua ferry group in the Xingan 523 block basement. Draft 524 References

525 Anderson J L,Morrison J. Ilmenite, magnetite, and peraluminous Mesoproterozoic anorogenic

526 granites of Laurentia and Baltica[J].Lithos,2005,80(1/4):45-60.

527 Belousova E A, Griffin W L, O'Reilly, et al. Igneouszircon: trace element composition as an

528 indicator of source rock type[J] . Contributions to Mineraloy and Petrology, 2002, 143:

529 602-622.

530 Biao Shang-hu, Li Yang-chun, He Xiao-hua, et al. The Geochemical Characteristics of the

531 Xinghuadukou Grop in the Lulin Forestry Center, Tahe, Hei-longjiang Province[J].Regional

532 Geology of China.1999,18(1):28-32

533 Burnham A D, Berry A J. An experimental study of traceelement partitioning between ziron and

534 melt as a function ofoxygen fugacity[J]. Geochimica et Cosmochimica Acta, 2012,

535 95:196−212.

https://mc06.manuscriptcentral.com/cjes-pubs Canadian Journal of Earth Sciences Page 26 of 46

536 Chen Yan-jing, Zhang Cheng, Li Nuo, et al. Geology of the Mo Deposits in Northeast China.

537 [J].Journal of Jilin University(Earth Science Edition) , 2012, 42(5):1223-1268.

538 Chen Zhi-guang, Zhang Lian-chang, Lu Bai-zhi, et al. Geochronology and Geochemistry of the

539 Taipingchuan Copper–Molybdenum deposit in Inner Mongolia, and its Geological

540 Significances[J].Acte Petrologica Sinica,2010,26(5):1437-1449.

541 Chen Zhi-guang, Zhang Lian-chang, Wu Ying-hua,e t al. Ar-Ar Age,Geochemistry and

542 Petrogenesis of Late Mesozoic Volcanic Rocks in the Northern Marginal Region of Erlian

543 Basin, Inner Mongolia[J]．Acta Petrologica Scinica, 2009，25( 2) : 297 － 310．

544 Cogné M, Morvan C L, Sirac C. Mammifère non-humain transgénique pour la région constante de 545 la chaîne lourde des IgA humainesDraft et ses applications (monoclonaux humanisés à destinée 546 muqueuse)[J]. 2005.

547 Collins W J, Beams S D, White A J R, et al. Nature and origin of A-type granites with particular

548 reference to southeastern Australia[J]. Contributions to Mineralogy & Petrology, 1982,

549 80(2):189-200.

550 Dall'Agnol R, Oliveira D C. Oxidized, magnetite-series, rapakivi-type granites of Carajas,

551 Brazil: Implication for classification and pet-rogenesis of A-typegranite[J].Lithos,

552 2007,93(3/4):215-233

553 Dong Ce,Zhou Jian-bo.Geochemistry of～500Ma Pan-African khondalite series in west of NE

554 China and tectonic implications[J].Acta Petrologica Sinica, 2012, 28(9):2866-2878.

555 Eby GN. 1992. Chemical subdivision of the A-type granite ids: petrogenetic and tectonic

556 implications. Geology, 20: 641- 644

557 Evans O C, Hanson G N. Accessory-mineral fraction of ra-reearth element abundance in granitoid

https://mc06.manuscriptcentral.com/cjes-pubs Page 27 of 46 Canadian Journal of Earth Sciences

558 rocks[J]. Chemical Geology, 1993, 110: 69- 93.

559 Fan W M ， Guo F ， Wang Y J ， et al. Late Mesozoic calcalkaline volcanic of post-orogenic

560 extension in the northern Da Hinggan Moutains ， northeatern China[J]. Journal of

561 Volcanology and Geothermal Research, 2003, 121:115-135．

562 Ge Wen-chun，Li Xian-hua，Lin Qiang，et al．Geochemistry of Early Cretaceous alkaline

563 rhyolites from Hulun-lake，Daxing'anling and its tectonic implications[J]．Geological

564 Sciences，2011，36 ( 2) : 176-183．

565 Ge Wen-chun，Lin Qiang，Sun De-you，et al. Geo-chemical characteristics of the Mesozoic

566 basalts in Da Hinggan Ling: evidence of the mantle-crust interaction[J]. Acta Petrologica 567 Sinica，1999，15 ( 3) : 397-407．Draft 568 Ge Wen-chun, Sui Zhen-min, Wu Fu-yuan, et al. Zircon U-Pb ages, Hf isotopic characteristics and

569 their implications of the Early Paleozoic granites in the northeastern Da Hinggan

570 Mts.,northeastern China[J].Acta Petrologica Sinica, 2007，23(2): 423 －440.

571 Ge Wen-chun,Wu Fu-yuan, Zhou Chang-yong,et al. Zircon U-Pb ages and its significance of the

572 Mesozoic granites in the Wulanhaote region, central Da Hinggan Mountain[J]. Acta

573 Petrologica Sinica,2005, 21(3):749-762.

574 Geology and Mineral Bureau of Inner Mongolia. Lithostratigraphy of Inner Mongolia[M] .Wuhan:

575 China University of Geosciences Press,1996: 256-264．

576 Gou Jun ， Sun De-you ， Zhao Zhong-hua ， et al ． Zircon LA-ICP-MS U-Pb dating and

577 petrogenesis of rhyolites in Baiyingaolao Formation from the southern Manzhouli ， Inner

578 Mongolia [J] ．Acta Petrologica Sinica，2010，26( 1) : 333-344．

https://mc06.manuscriptcentral.com/cjes-pubs Canadian Journal of Earth Sciences Page 28 of 46

579 Guo Zhi-jun, Li Jin-wen, Huang Guang-jie, et al. Sr-Nd-Pb-Hf isotopic characteristics of

580 ore-bearing granites in the Honghuaerji scheelite deposit, Inner Mongolia[J].Geology in

581 China ,2014, 41(4):1226-1241.

582 Hanson J N. The application of trace-elements to the petro-genesis of igneouse rocks of granitic

583 composition[J]. Earthand Planetary Science Letters, 1978, 38: 26- 43.

584 Heilongjiang Bureau of Gology and Mineral Resources. Regional Geology of Heilongjiang

585 Province[M].Beijing: Geological Publishing House,1993:1-734.

586 Hong Da-wei, Wang Shi-guang, Xie Xi-lin, et al. Genesis of positive ε(Nd,t) granitoids in the Da

587 Hinggan Mountains[J].Earth Science Frontiers, 2000,7(2):441-456. 588 Hoskin P W O, Schaltegger U. TheDraft composition of zirconand igneous and metamorphic 589 petrogenesis[J]. Reviews in Mineralogyand Geochemistry,2003,53(1):27-55.

590 Huang Ming-da, Cui Xiao-zhuang, Pei Sheng-liang, et al. Rhyolite Zircon U-Pb Dating and Its

591 Tectonic Significance in Bayan Gol Formation, Hinggan Massif[J]. Coal Geology Of China,

592 2016, 28(11):30-37.

593 Inner Mongolia Bureau of Geology and Mineral Resources. Regional geology of Inner

594 Mongolia[M].Beijing: Geological Publishing House, 1991：1-725

595 Jiang Si-hong, Nie Feng-jun, Su Yong-jiang, et al. Geochronology and Origin of the Erdenet

596 Superlarge Cu-Mo Deposit in Mongolia [J] .Acta Geoscientica Sinica，2010.，31(3): 289－

597 306.

598 Jochum K P.Snow J E, Snow J E. Nb/Ta in mantle and crust[J].EOS,1997,78:804.

599 King P L, White AJR, Chappell B W, et al.1997.Characterization and origin of aluminous A-type

600 granites from the Lachlan Fold Belt, southeastern Australia.J.Petrol.,38:371-391.

https://mc06.manuscriptcentral.com/cjes-pubs Page 29 of 46 Canadian Journal of Earth Sciences

601 Koschek G. Origin and significance of the SEM cath-odoluminescence from zircon [J]. Journal of

602 Microscopy，1993，171 ( 3) : 223-232．

603 Kravchinsky V A, Cogné J P, Harbert W P, et al. Evolution of the Mongol-Okhotsk Ocean as

604 constrained by new palaeomagnetic data from the Mongol-Okhotsk suture zone, Siberia[J].

605 Geophysical Journal International, 2002, 148(1):34–57.

606 Li Jin-yi, Gao Li-ming, Sun Gui-hua, et al. Shuangjingzi middle Triassic syn-conllisional

607 crust-derived granite in the east Inner Mongolia and its constraint on the timing of collision

608 between Siberian and Sino-Korean paleo-plates[J].Acta Petrologica Sinica, 2007,

609 23(3):565-582. 610 Lin Qiang, Ge Wen-chun, Sun De-you,Draft et al. Tectonic significance of Mesozoic volcanic rocks in 611 Northeastern China[J]. Scientia Geologica Sinica 1998(2):129-139.

612 Litvinovsky B A, Steel I M and Wickham S M. 2000. Silicic magma formation in overthickened

613 crust: melting of charnockite and leucogranite at 15, 20 and 25 kbar[ J]. Journal of Petrology,

614 41:717～ 737.

615 Liu Jian-feng, Li Jin-yi, Sun Li-xin, et al. Zircon U- Pb dating of the Jiujingzi ophiolite in Bairin

616 Left Banner, Inner Mongolia: Constraints on theformation and evolution of the Xar Moron

617 River suture zone[J]. Geology in China, 2016, 43(6): 1947-1962(in Chinese with English

618 abstract).

619 Liu Xiao-guang.T he Geological-Geochemical Characteristics and the Structural Significance of

620 the Xinghuadukou Rock Group of Paleoproterzoic in Heihe Area. [D].Jilin University,2007.

621 Loiselle M C and Wones D .1979.Characteristics and origin of anoro-genic granites[J].Geological

622 Society of America,Abstracts with Programs,11:468.

https://mc06.manuscriptcentral.com/cjes-pubs Canadian Journal of Earth Sciences Page 30 of 46

623 Martin H, Smithies R H, Rapp R, et al. An overview of adakite,

624 tonalite–trondhjemite–granodiorite (TTG), and sanukitoid: relationships and some

625 implications for crustal evolution[J]. Lithos, 2005, 79(1–2):1-24.

626 Martin RF．2006． A-type granites of crustal origin ultimately result fromopen-system

627 fenitization-type reactions in an extensional environment． Lithos， 91: 125－136

628 Mass R, Kinny P D, Williams I S, et al. The Earth's oldest kown crust: A geochronological and

629 geochemical study of 2900-4200 Ma old detrital zircons from Mt.Narryer and Jack

630 Hills,Weastern Australia[J]. Geochimica et Cosmochimica Acta,1992,56:1281-1300.

631 Mass R, Kinny P D, Williams I S, et al. The Earth's oldest kown crust: A geochronological and 632 geochemical study of 2900-4200 MaDraft old detrital zircons from Mt.Narryer and Jack Hills, 633 Weastern Australia[J]. Geochimica et Cosmochimica Acta,1992,56:1281-1300.

634 Mc Donough W F, Sun S-s. The composition of the Earth[J]. Chem Geol,1995,120(3/4):223-253.

635 Meng En， XuWen-liang， Yang De-bin， et al． Zircon U --Pb chronology， geochemistry

636 of Mesozoic volcanicrocks from the Lingquan basin in Manzhouli area ， and itstectonic

637 implications [J] ． Acta Petrologica Sinica，2011， 27 ( 4) : 1209-1226．

638 Xu Mei-Jun, Xu Wen Liang, Meng En, et al. LA-ICP-MS zircon U-Pb chronology and

639 geochemistry of Mesozoic volcanic rocks from the Shanghulin-Xiangyang basin in Ergun

640 area,northeastern Inner Mongolia.Geological Bulletin of Chia,2011,30(9):1321-1338

641 Meng Q R. What drove Late Mesozoic extension of thenorthen China Mongolia

642 tract[J]．Tectonophysics，2003，369: 155-174．

643 Metelkin D V, Vernikovsky V A, Kazansky A Y, et al. Late Mesozoic tectonics of Central Asia

644 based on paleomagnetic evidence[J]. Gondwana Research, 2010, 18(2):400-419.

https://mc06.manuscriptcentral.com/cjes-pubs Page 31 of 46 Canadian Journal of Earth Sciences

645 Miao Lai-cheng, Fan Wei-ming, Zhang Fu-qin, et al. Zircon SHRIMP geochronology of the

646 Xingkailing-Kele complex in the northwestern Lesser Xing’an Range,and its geological

647 implication[J].Chinese Sci Bull, 2003, 48(22):2315-2323.

648 Mou Bao-lei. Element Geochemistry.[M].Beijing University Press,1999

649 Murry et al.1990, Rare earth elements as indicators of different marine depositional environments

650 in chert and shale,Geology,18,268-271.

651 Nie Li-jun, Jia Hai-ming, Wang Chong, et al. Chronology, geochemistry of rhyolites from

652 Baiyingaolao Formation in the middle part of Da Hinggan Mountains and its tectonic

653 implications[J].Global Geology，2015，34（2）：296-304. 654 Parfenov L M，Popeko LI and TomurtogooDraft O. 2001. Problems of tectonics of the 655 Mongol-Okhotsk orogenic belt. Geology of the Pacific Ocean，16: 797 － 830

656 Patino Douce A E. Generation of metaluminous A-type granites by low-pressure melting of

657 calc-alkaline granitoids.[J]. Geology, 1997, 25(8):743-746.

658 Patino Douce AE. 1999. What do experiments tell us about the relative contributions of crus t and

659 mantle to the origin of granitic magmas. In: Castro A, Fernandez C& Vegeress e JL ( ed s. ):

660 Understanding Granites In tegrating New and Classical Techniques. The Geological Society,

661 London, Special Publications. 168: 55- 75

662 Pei J, Sun Z, Jing L, et al. A paleomagnetic study from the Late Jurassic volcanics (155 Ma),

663 North China: Implications for the width of Mongol–Okhotsk Ocean[J]. Tectonophysics,

664 2011, 510(3–4):370-380.

https://mc06.manuscriptcentral.com/cjes-pubs Canadian Journal of Earth Sciences Page 32 of 46

665 Qin Tao, Zheng Chang-qing, Cui Tian-ri, et al. Volcanic rocks of the Baiyingaolao Formation in

666 the Southwest of Zhalantun, Inner Monogolia :Geochemistry, Geochronology and Tectonic

667 Implications. [J].Geology and Resources, 2014, 23(2):146-153.

668 Rajesh H M． 2000． Characterization and origin of a compositionally zoned aluminous A-type

669 granite from South India． Geological Magazine，137( 3) : 291 － 318

670 Reid J B J, Murray D P, Hermes O D, et al. Fractional crystallization in granites of the Sierra

671 Nevada: How important is it?[J]. Geology, 1993, 21(7):587.

672 Ren Jisun, Wang Zuoxun, Chen Bingwei, et al. The Tectonics of China from a Giobal View :A

673 Guide to the Tectonic Map of China and Adjacent Regions[M].Beijing:Geological Publishing 674 House,1999:4-32 Draft 675 Sao Ji-an, Liu Fu-tian, Chen Hui, et al. Relationshipbetween Mesozoic magmatism and subduction

676 in Da Hing-gan-Yanshan area[J]．Acta Geologica Sinica，2001，75( 1) : 56-63．

677 Şengör A M C, Natal'in B A,Burtman V S.Evolution of the Altaid tectonic collage and Palaeozoic

678 crustal growth in Eurasia[J].Nature,1993,364(6435):299-307.

679 Shao Ji-an, Zhang Lu-qiao. Magmatism in the Mesozoic Extending Orogenic Process of Hinggan

680 Mts. [J] Earth Science Frontiers,1999,6(4):339-346

681 Shao Ji-an, Zhang Lu-qiao. Magmatism in the Mesozoic Extending Orogenic Process of Hinggan

682 Mts. [J] Earth Science Frontiers,1999,6(4):339-346

683 Si Qiu-liang, Cui Tian-ri, Tang Zhen, et al. Chronology ,Gechemistry and Petrogensis of the

684 Volcanic Rocks in Manitu Formation in Chaihe Area,Central Great Xing’an Range.Journal of

685 Jilin University :Earth Science Edition，2015,45（2）:389-403.

https://mc06.manuscriptcentral.com/cjes-pubs Page 33 of 46 Canadian Journal of Earth Sciences

686 Skjerlie K P, Johnston A D. Vapor-absent melting at 10 kbar of a biotite- and amphibole-bearing

687 tonalitic gneiss: Implications for the generation of A-type granites[J]. Geology, 1992,

688 20(3):263-266.

689 Sun Guang-rui, Li Yang-chun ,Zhang Yu. The basement tectonics of ergun massif. [J].Geology

690 and Resources,2002,(03):129-139.

691 Sun S-s, Mc Donough W F. Chemical and isotopic systematics of oceanic basalts: Implications for

692 mantle composition and processes[M].//Saunders A D. Norry M J. Magmatism in the Ocean

693 Basins. Geol Soc Spec Pub 42,1989:313-345.

694 Turner Sand RushmerT.2010.Similarities between mantle-derived A-type granites and voluminous 695 rhyolites in continental flood basaltDraft provinces[J].Transactions of the Royal Society of 696 Edinburgh, Earthand Environmental Science,100:1~10.

697 Wang Cheng-wen, Jin Wei, Zhang Xing-zhou, et al. New understanding of the Late Paleozoic

698 tectonics in northeastern China and adjacent areas[J]. Journal of Stratigraphy, 2008,

699 32(2):119-136 (in Chinese with English abstract).

700 Wang F, Zhou X H, Zhang L C, et al. Late Mesozoic volcanism in the Great Xing'an Range(NE

701 China):timing and implications forthe dynamic setting of NE Asia[C]. Summary of 2006

702 papers by Institute of Geology and Geophysics, Chinese Academy of Sciences.

703 2007:179-198.

704 Wang Jian-guo, He Zhong-hua, Xu Wen-liang. Petrogenesis of riebeckite rhyolites in the southern

705 Da Hinggan Mts: Geohronological and geochemical evidence[J]. Atca Petrologica Sinica,

706 2013, 29(3):853-863.

707 Wang Y，Zhang FQ，Zhang DW，Miao LC，Li TS，Xie HQ，Meng QR and Liu DY．2006．

https://mc06.manuscriptcentral.com/cjes-pubs Canadian Journal of Earth Sciences Page 34 of 46

708 Zircon SHRIMP U-Pb dating of meta-diorite from the basement of the Songliao basin

709 and its geological significance. Chinese Science Bulletin，51: 1877 － 1883

710 Wang Yang, Jiao Yong-ling, Tong Li-hua, et al. The essence of A-type granitoids: A discussion

711 on the opinions held by Prof. Zhang Qi and some other researchers[J].Acta Petrologica Et

712 Mineralogica. , 2013, 32(2):260-266.

713 Watson E B，Harrison T M．Zircon saturation revisited:temperature and composition effect in

714 avariety of crustalmagmas types[J].Earth and Planetary Science Letters，1983，64: 295-304．

715 Wei-wei, Wang Guo-qi, Wang Li-jia, et al. The protolith restoration and formation environment of

716 discussion of paleoproterozoic Xinghuadukou group Xinghus litho formation in Mohe 717 areas.[J]. China Academic JournalDraft Electronic Pushing House.，2016,3：43-44. 718 Whalen J B, Currie K Land Chappell B W. 1987.A-type granites: geochemical characteristics,

719 iscriminations and petrogenesis[ J]. Contributions to Mineralogy and Petrology, 95: 407～

720 419.

721 Wu F Y, Li X H, Yang J H, et al. Discussions on the petrogenesis of granites[J]. Acta Petrologica

722 Sinica, 2007, 23(6):1217-1238.

723 Wu F Y, Sun D Y, Ge W C, et al. Geochronology of the Phanerozoic granitoids in northeastern

724 China[J]. Journal of Asian Earth Sciences, 2011, 41(1):1-30.

725 Wu F Y, Sun DY, Li HM , Jahn BM and Wilde S.2002.A-type granites in northeastern China: Age

726 and geochemical constraints on their petrogenesis. Chemical Geology,187:143-173.

727 Wu G, Chen Y, Chen Y, et al. Zircon U–Pb ages of the metamorphic supracrustal rocks of the

728 Xinghuadukou Group and granitic complexes in the Argun massif of the northern Great

https://mc06.manuscriptcentral.com/cjes-pubs Page 35 of 46 Canadian Journal of Earth Sciences

729 Hinggan Range, NE China, and their tectonic implications[J]. Journal of Asian Earth

730 Sciences, 2012, 49(3):214-233.

731 Wu Jun. Geological age and geochemical characteristics of alkline rhyolites at Hongshanzi basin

732 in south Great Hingan Range[D].East China Institute of Technology, 2013.

733 Xu W L, Ji W Q, Pei F P, et al. Triassic volcanism in eastern Heilongjiang and Jilin provinces, NE

734 China: Chronology, geochemistry, and tectonic implications[J]. Journal of Asian Earth

735 Sciences, 2009, 34(3):392-402.

736 Xu Wen-liang， Wang Feng， Pei Fu-ping， et al． Mesozoic tectonic regimes and regional

737 ore-forming background in NE China: constraints from spatial and temporal variations of 738 Mesozoic volcanic rock associations[J]Draft ． Acta Petrologica Sinica， 2013， 29 ( 2 ) : 739 339-353．

740 Xu Wen-liang，Ge Wen-chun，Pei Fu-ping，et al． Geochronological framework and tectonic

741 significance of Mesozoic volcanism in northeastern China [J]． Bulletin of Mineralogy，

742 Petrology and Geochemistry，2008，27( Suppl．) : 286-287．

743 Zeng Wei-shun, Zhou Jian-bo, Dong Ce, et al. Subduction record of Mong-Okhotsk Ocean:

744 Constrains from Badaguan metamorphic complexes in the Erguma massif, NE China. [J].

745 Acte Petrologica Sinica, 2014, 30(7):1948-1960.

746 Zeng Wei-shun ,Zhou Jian-bo, Dong Ce, et al. Subduction record of Mongol-Okhotsk Ocean:

747 Constrains from Badaguan metamorphic complexes in the Erguna massif, NE China.[J].Acta

748 Petrologica Sinica,2014,30(7):1948-1960.

749 Zhang J H, Ge W C, Wu F Y, et al. Large-scale Early Cretaceous volcanic events in the northern

750 Great Xing'an Range, Northeastern China[J]. Lithos, 2008, 102(1–2):138-157.

https://mc06.manuscriptcentral.com/cjes-pubs Canadian Journal of Earth Sciences Page 36 of 46

751 Zhang J H, Gao S Ge W C, et al. Geochronology of the Mesozoic volcanic rocks in the Great

752 Xing'an Range，northeastern China: implications for subductiion-induceddelamination [J]．

753 Chemical Geology，2010，276: 144-165．

754 Zhang Ji-heng. Geochronology and geochemistry of the Mesozoic volcanic rocks in the Great

755 Xing’an Range, northeastern China. [D] ．Beijing: China University of Geosciences,2009.

756 Zhang Le-tong，Li Shi-chao，Zhao Qing-ying,et al. Formation age and geochemical

757 characteristics of volcanic rocks from Baiyingaolao Formation of middle Da Hinggan

758 mountains[J]. Global Geology, 2015，34（01）：1004-5589.

759 Zhang Qi， Ran Hao， Li Cheng-dong． A-type granite: What is the essence? [J] ． Acta 760 Petrologica et Mineralogica， 2012Draft， 31 ( 4) : 621-626． 761 Zhang Qi, Pan Guo-qiang, Li Cheng-dong , et al. Are discrimination diagrams always indicative

762 of correct tectonic settings of granites? Some crucial questions on granite study(3). [J].Acta

763 Petrologica Sinica, 2007，23 ( 11 ) : 2683-2698.

764 Zhang Qi, Wang Yan, Li Cheng-dong, et al. Granite classification on the basis of Sr and Yb

765 contents and its implications.[J]Acta Petrologica Sinica,2006,22(9):2249-2269 .

766 Zhang Xiang-xin, Gao Yong-feng, Lei Shi-he. Zircon U-Pb age and geochemistry of shoshonitic

767 rocks from the Manitu Formation in the Honggeer area, central Inner Mongolia and their

768 geological significance.[J] ．Geochimica. ，2016，, 45,（4）： 356~373

769 Zhang Xing-zhou, Yang Bao-jun, Wu Fu-yuan, et al. The lithosphere structure in the

770 Hingmong-Jihei(Hinggan-Mongolia-Jilin-Heilongjiang)region,northeastern

771 China[J].Geology In China, 2006, 33(4):816-823.

https://mc06.manuscriptcentral.com/cjes-pubs Page 37 of 46 Canadian Journal of Earth Sciences

772 Zhang Xue-bin，Zhou Chang-hong，Lai Lin,et al． Geo-chemistry and zircon U- Pb dating of

773 volcanic rocks in eastern Xilin Hot，Inner Mongolia and their geological implications[J]．

774 Geology and Exploration，2015，51( 2) : 0290 － 0302．

775 Zhao Guo-long, Yang Gui-lin, Wang Zhong. Volcanic rocks in the central-southern Da Hinggan

776 Mountains[ M]．Beijing: Beijing Science and Technology Pushlishing House,1989:1-252

777 Zhao Yue, Yang Zhen-ning, Ma Xing-hua.Geoteconic transition from paleoasian system and

778 Paleotethyan system to paleo-pacific active continental margin in eastern Asia [J] .Scientia

779 Geologica Sinica, 1994(2):105-119.

780 Zhao Zheng-hua, Zhou ling-li. REE geochemistry of some alkali-rich intrusive rocks in China[J]. 781 Science in China(Series D:Earth Sciences),1997,(02):145-158.Draft 782 Zhao Zhen-hua, Xiong Xiao-lin, Wang Qiang, et al.S ome aspects on geochemistry of Nb and

783 Ta[J].Geochemical, 2008, 37(4):304-320.

784 Zhou J B, Wilde SA. The crustal accretion history and tectonic evolution of the NE China segment

785 of the Central Asian Orogenic Belt[J]. Gondwana Research, 2013, 23(4):1365-1377.

786 Zhou JB ， Wilde SA ， Zhang XZ ， Ren SM and Zheng CQ. 2011b. Early Paleozoic

787 metamorphic rocks of the Erguna block in the Great Xing’an Ｒange， NE China: Evidence

788 for the timing of magmatic and metamorphic events and their tectonic implications.

789 Tectonophysics，499( 1－4) : 105－117

790 Zhou JB， Wilde SA， Zhang XZ， Zhao GC， Liu FL, Qiao DW， Ren SM and Liu JH.

791 2011a. A ＞ 1300km Late Pan-African metamorphic belt in NE China: New evidence from

792 the Xing’ an block and its tectonic implications. Tectonophysics，509( 3-4) : 280－292

https://mc06.manuscriptcentral.com/cjes-pubs Canadian Journal of Earth Sciences Page 38 of 46

793 Zhou Jian-bo, Shi Ai-guo, Jing Yan. The Combined NE China Blocks: Tectonic Evolution and

794 Supercontinent Reconstrutions. Journal of Jilin University (Earth Science Edition)，2016,46（4

795 ）1042-1055.

796 Zonenshain L P, Kuzmin M I, Natapov L M, et al. Geology of the USSR: A Plate-Tectonic

797 Synthesis[J]. Amer. geophys. union Geodynamics, 1990, 21.

798

Draft

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Table1 Rare Earth Element Test Data of Zircon ( × 10 - 6 ) and Its Parameters

Sample I01 I02 I03 I04 I05 I06 I07 I08 I09 I10 I11 I12 I13 I14 I15 I16 I17 I18 I19 I20 I21 I22 I23 I24 I25 I26 I27 I28 I29 La 0.04 0.09 0.04 0.05 0.05 0.05 0.05 0.01 15.18 0.04 0.03 0.02 0.03 7.03 0.00 0.02 0.68 1.54 0.30 0.03 0.06 0.09 8.58 0.43 0.22 0.01 0.03 0.04 0.03 Ce 420 352 205 314 342 420 269 180 320 171 401 375 203 281 308 316 179 289 151 390 412 262 473 263 276 289 253 401 162 Pr 0.43 0.47 0.51 0.42 0.40 0.73 0.78 0.21 5.35 0.21 0.35 0.30 0.38 2.60 0.32 0.31 0.51 0.92 0.32 0.31 0.49 0.30 5.48 0.52 0.73 0.40 0.40 0.42 0.30 Nd 7.69 7.52 8.64 7.38 6.29 7.37 12.22 4.25 27.81 4.03 7.74 6.77 6.24 17.25 6.83 6.25 6.87 11.24 4.35 7.67 9.34 6.08 32.08 8.07 9.30 6.61 6.70 7.98 5.47 Sm 21.39 19.70 18.15 18.36 17.63 20.99 24.42 11.01 25.11 10.91 21.37 19.67 13.51 21.99 16.26 16.42 13.61 21.56 10.38 20.15 22.72 15.19 29.38 17.37 20.87 16.88 16.61 20.53 12.90 Eu 5.44 4.78 4.68 4.66 4.53 5.54 6.06 2.87 5.54 2.79 5.39 4.70 3.59 5.10 4.00 4.30 3.58 5.51 2.87 5.16 5.59 3.89 6.35 4.21 4.87 4.44 4.07 5.05 3.33 Gd 110 102 93 99 92 115 124 60 103 55 105 98 76 101 88 86 72 104 56 101 115 77 120 85 100 89 80 103 65 Tb 39 36 33 35 33 39 44 23 37 21 37 34 28 37 30 32 27 38 22 35 41 30 40 31 37 33 29 37 25 Dy 440 402 382 400 374 427 496 267 417 252 415 382 324 415 347 368 310 437 269 402 460 346 447 367 420 385 340 408 293 Ho 156 142 136 144 133 148 175 100 148 92 145 133 Draft119 149 125 134 114 155 102 140 162 125 155 132 150 141 121 142 107 Er 645 586 574 601 554 587 719 424 618 397 591 542 501 616 513 561 477 638 435 566 664 524 620 554 611 578 507 578 457 Tm 124 112 111 116 107 110 137 84 119 80 112 102 98 120 100 109 94 124 86 107 127 103 116 107 118 111 99 108 89 Yb 1075 980 973 1019 931 943 1188 747 1042 703 956 884 854 1040 863 966 819 1072 763 921 1094 896 994 942 1018 981 867 921 805 Lu 185 168 169 175 160 161 203 131 181 123 162 150 150 181 147 168 142 187 135 157 186 157 169 165 177 171 150 156 138 Y 4596 4226 4095 4292 3959 4341 5020 2957 4372 2770 4295 3979 3532 4378 3733 3980 3326 4631 2980 4153 4892 3693 4595 3906 4422 4141 3649 4233 3218 ΣREE 3230 2911 2708 2934 2755 2985 3399 2033 3063 1912 2958 2731 2376 2993 2548 2768 2259 3084 2038 2852 3299 2545 3216 2677 2942 2807 2473 2888 2164 LREE 455 384 237 345 371 455 312 198 399 189 436 406 227 335 336 343 205 330 170 423 450 288 555 294 312 317 281 435 184 HREE 2774 2527 2470 2589 2384 2530 3087 1835 2664 1723 2522 2324 2149 2658 2212 2425 2054 2755 1869 2428 2849 2257 2661 2384 2630 2490 2192 2453 1979 LREE/ 0.16 0.15 0.10 0.13 0.16 0.18 0.10 0.11 0.15 0.11 0.17 0.17 0.11 0.13 0.15 0.14 0.10 0.12 0.09 0.17 0.16 0.13 0.21 0.12 0.12 0.13 0.13 0.18 0.09 HREE δEu 0.28 0.26 0.28 0.27 0.28 0.27 0.27 0.27 0.29 0.28 0.28 0.27 0.27 0.28 0.26 0.28 0.28 0.29 0.29 0.29 0.27 0.28 0.28 0.28 0.27 0.28 0.28 0.27 0.29 δCe 296 216 121 220 254 175 105 259 9 230 342 375 161 16 300 315 72 58 108 384 250 242 16 118 105 221 189 285 165

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Table 2 Zircon U–Pb analytical data for rich Nb-Ta rhyolite.

Pb Th U 207Pb/206Pb 207Pb/235U 206Pb/238U 207Pb/206Pb 207Pb/235U 206Pb/238U

Isotope Isotope Isotope Age Age Age

Point (×10-6) Th/U Ratio 1σ Ratio 1σ Ratio 1σ (Ma) 1σ (Ma) 1σ (Ma) 1σ

I-1 20 1221 707 1.73 0.048340.001840.11951 0.0049 0.017930.00048 116 50 115 4 115 3

I-2 17 1084 609 1.78 0.048290.001970.116760.005090.017530.00047 114 55 112 5 112 3

I-3 8 389 313 1.24 0.048320.002270.118970.005840.017850.00049 115 65 114 5 114 3

I-4 14 799 512 1.56 0.04838 0.0022 0.119850.005750.017960.00049 118 63 115 5 115 3

I-5 16 923 591 1.56 0.048330.002260.117740.005770.017670.00049 115 64 113 5 113 3

I-6 23 1594 759 2.10 0.04835 0.0021 0.11979 0.0055 0.017970.00049 116 59 115 5 115 3

I-7 11 564 396 1.42 0.048410.002370.120690.006170.018080.00049 119 69 116 6 116 3

I-8 8 344 307 1.12 0.048220.002520.120720.006540.01815 0.0005 110 74 116 6 116 3

I-9 11 515 403 1.28 0.048070.004480.118290.011010.017850.00056 103 148 114 10 114 4

I-10 8 315 300 1.05 0.048530.005770.119110.01419 0.0178 0.00054 125 210 114 13 114 3

I-11 21 1531 769 1.99 0.048360.002580.118330.006510.01774 0.0005 117 75 114 6 113 3

I-12 22 1563 753 2.08 0.04825 0.0016 0.115660.004240.017380.00046 112 42 111 4 111 3

I-13 8 382 322 1.19 0.048270.002560.119090.006530.01789 0.0005 113 75 114 6 114 3

I-14 10 508 389 1.30 0.048330.003720.120440.009390.018070.00051 115 122 115 9 115 3 I-15 17 1047 576 1.82 0.0483 0.00269Draft0.117960.006730.01771 0.0005 114 79 113 6 113 3 I-16 13 638 488 1.31 0.048360.002690.119350.00686 0.0179 0.00049 117 81 114 6 114 3

I-17 8 381 301 1.26 0.048150.003250.116970.008070.017620.00049 107 103 112 7 113 3

I-18 12 689 448 1.54 0.048220.002180.118380.00561 0.0178 0.00049 110 61 114 5 114 3

I-19 7 286 271 1.06 0.048220.003380.11928 0.0085 0.017940.00051 110 107 114 8 115 3

I-20 24 1667 812 2.05 0.048280.002030.119180.00534 0.0179 0.00048 113 57 114 5 114 3

I-21 20 1263 717 1.76 0.04829 0.0022 0.120610.005780.018110.00049 114 63 116 5 116 3

I-22 11 522 414 1.26 0.04815 0.002 0.12024 0.0053 0.018110.00049 107 55 115 5 116 3

I-23 26 1869 861 2.17 0.048280.001870.117830.00491 0.0177 0.00048 113 51 113 4 113 3

I-24 10 426 377 1.13 0.048370.003630.118590.009010.017780.00051 117 117 114 8 114 3

I-25 11 551 440 1.25 0.048070.003670.118020.009130.017810.00051 103 119 113 8 114 3

I-26 11 555 444 1.25 0.04832 0.0025 0.118210.006340.017740.00049 115 73 113 6 113 3

I-27 11 568 417 1.36 0.048370.002830.119260.007160.017880.00051 117 85 114 6 114 3

I-28 24 1653 791 2.09 0.048380.002080.118630.005410.017780.00049 118 58 114 5 114 3

I-29 7 316 272 1.16 0.0483 0.003260.118830.008150.017840.00051 114 101 114 7 114 3

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Table3 Contents of major elements(wt%) and trace elements(ppm) of rich Nb-Ta rhyolite

Sample I-1 I-2 I-3 I-4 I-5 I-6 I-7 Ave

SiO2 72.66 72.37 73.22 73.00 72.82 72.35 72.63 72.72

Al2O3 13.23 13.25 13.18 13.38 13.18 13.42 13.60 13.32

Fe2O3 1.70 1.66 1.37 1.49 1.67 1.62 1.86 1.62 FeO 0.09 0.09 0.37 0.19 0.14 0.14 0.68 0.24 CaO 0.17 0.17 0.17 0.16 0.18 0.18 0.12 0.16 MgO 0.07 0.06 0.08 0.04 0.07 0.06 0.06 0.06

K2O 7.80 7.78 5.51 5.61 6.97 7.43 4.81 6.56

Na2O 3.61 3.65 5.34 5.16 3.99 3.91 4.58 4.32

TiO2 0.18 0.17 0.18 0.18 0.17 0.17 0.19 0.18

P2O5 0.01 0.01 0.02 0.03 0.02 0.01 0.02 0.02 MnO 0.04 0.04 0.12 0.06 0.02 0.01 0.09 0.05 LOI 0.40 0.41 0.26 0.35 0.44 0.37 0.68 0.42 Total 99.97 99.67 99.82 99.64 99.65 99.68 99.32 99.68 TFeO 1.62 1.58 1.60 1.53 1.64 1.60 2.35 1.70 TFeO/(TFeO+MgO） 0.96 0.96 0.95 0.97 0.96 0.96 0.98 0.96 A/NK 0.92 0.92 0.89 0.92 0.93 0.93 1.07 0.94 A/CNK 0.90 0.90 0.88 0.90 0.91 0.91 1.05 0.92 La 21.16 23.33 21.19 19.51 15.27 26.8 24.38 21.66 Ce 44.89 50.46 52.94 45.64 32.59 56.76 82.66 52.28 Pr 4.69 5.06 4.10 4.64 3.53 4.95 4.65 4.52 Nd 15.26 16.43 12.48 15.26 12.24 16.02 16.38 14.87 Sm 3.38 3.58 2.34 3.38 3.08 3.11 4.14 3.29 Eu 0.51 0.50 0.32 0.46 0.41 0.4 0.58 0.45 Gd 3.58 3.67 2.18 3.61 3.41 3.63 4.87 3.56 Tb 0.83 0.84 Draft0.50 0.81 0.77 0.91 1.19 0.84 Dy 5.34 5.67 3.19 5.63 5.31 6.64 8.47 5.75 Ho 1.36 1.39 0.86 1.39 1.29 1.44 1.74 1.35 Er 3.98 4.05 2.51 4.12 3.73 4.48 5.19 4.01 Tm 0.64 0.66 0.45 0.65 0.59 0.75 0.85 0.66 Yb 4.27 4.50 3.35 4.65 4.04 5.12 5.78 4.53 Lu 0.69 0.68 0.56 0.71 0.62 0.74 0.84 0.69 ΣREE 110.57 120.81 106.96 110.46 86.87 131.75 161.72 118.45 LREE/HREE 4.35 4.63 6.87 4.12 3.40 4.56 4.59 4.65 LaN/YbN 3.56 3.72 4.54 3.01 2.71 3.76 3.03 3.47 δEu 0.44 0.42 0.43 0.40 0.39 0.36 0.39 0.40 δCe 1.06 1.09 1.31 1.14 1.05 1.21 1.9 1.25 Y 23.08 25.01 12.62 23.13 24.71 46.79 33.85 27.03 Be 3.16 3.19 7.59 7.34 4.28 3.96 7.05 5.22 Sc 2.50 2.56 2.77 2.84 2.68 2.04 2.24 2.52 V 0.24 0.21 0.08 0.08 0.16 5.03 1.56 1.05 Cr 0.29 0.41 0.07 0.34 0.16 5.29 5.7 1.75 Co 0.24 0.24 0.18 0.20 0.21 2.52 2.28 0.84 Ni 0.23 0.77 0.03 0.39 0.01 3.12 2.82 1.05 Cu 0.78 1.81 1.31 0.81 0.94 3.23 5.8 2.10 Zn 68.23 72.69 106.90 75.24 82.66 69.3 127 86.00 Ga 23.16 24.32 24.51 24.80 24.43 24.4 25.3 24.42 Rb 320.60 325.90 237.60 237.10 298.30 247 238 272.07 Sr 4.80 2.41 4.45 3.35 4.27 1.86 8.8 4.28 Ba 10.54 10.53 6.99 12.32 8.50 35.3 26.6 15.83 Nb 98.74 98.13 99.57 99.51 93.47 85.7 92.3 95.35 Ta 13.72 12.34 12.19 11.77 10.97 5.75 6.38 10.45 Zr 482.50 454.40 494.70 543.70 447.90 543 643 515.60 Hf 15.70 14.57 16.29 17.19 15.52 19.6 20.6 17.07 Th 18.90 20.96 20.00 21.17 16.21 15 21.6 19.12 U 3.87 3.91 3.80 4.05 3.18 3.28 2.78 3.55 Pb 17.25 17.74 26.19 38.73 21.48 28 50.2 28.51

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Table4 Sr-Nd isotopic results of rich Nb-Ta rhyolite.

87 86 87 86 147 144 143 /144 87 86 143 144 Rb/ Sr Sr/ Sr Sm/ Nd Nd Nd t/Ma εSr(0) εSr(t) fRb/Sr ( Sr/ Sr)ⅰ εNd(0) εNd(t) fSm/Nd TDM T2DM ( Nd/ Nd)

I -1 199.72 1.049779 0.1402 0.1401963 114 4901.05 310.16 2413.98 0.72621 0.61 1.4 -0.29 1005 799 0.512562ⅰ I -3 200.21 1.048341 0.1187 0.118676 114 4880.64 278.36 2413.96 0.72397 0.8 1.9 -0.40 758.0 754. 0.512590

I -4 211.58 1.047149 0.1402 0.140238 114 4863.72 -0.01 2557.41 0.70437 0.6 1.4 -0.29 1005 7990 0.512562 I -5 208.95 1.052516 0.1591 0.159132 114 4939.90 136.78 2525.56 0.71400 0.76 1.2 -0.19 1339 813 0.512553

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1 2 Fig.1 SimplifiedDraft geological map and Sampling position 3 4

5 6 Fig.2 Hand specimen photograph (a) 、photomicrograph of rich Nb-Ta rhyolite(b)、pyrochlore(c) and 7 titanomagnetite(d)

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8 9 Fig.3. CL images of zircons from rich Nb-Ta rhyolite 10 11 Draft

12 13 Fig.4 Zircon Chondrite-normalized REE distribution patterns (a) and LA–ICP-MS zircon U–Pb concordia 14 diagrams(b) of rich Nb-Ta rhyolite 15 16

17 18

19 Fig.5 Plots of SiO2 versus (SiO2 +K2O)(a)、Plots of A/CNK versus A/NK (b) and Plots of SiO2 versus K2O(c) for 20 rich Nb-Ta rhyolite

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21 22 Fig.6 Chondrite-normalized REE patterns (a) primitive mantle-normalized spidergram(b) of rich Nb-Ta 23 rhyolite 24 25

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26 27 Fig.7 Diagrams for discriminating tectonic setting of R1-R2(a)、Yb-Ta(b) and Hf-Rb/30-Ta×3(c) for rich Nb-Ta 28 rhyolite 29 30

31 32 Fig.8 Diagrams for genetic types(a、b、c、d) and Diagrams for discriminating tectonic setting(e、f) of rich Nb-Ta 33 rhyolite

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-6 36 Fig.9 Diagrams for La×10 versus La/Sm(a) and SiO2-(TFeO+MgO+TiO2) versus (TFeO+MgO+TiO2)(b) of rich 37 Nb-Ta rhyolite 38 39

Draft

40 41 Fig.10 Diagrams for rare earth elements (a) and trace elements (b).

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