draft · 2020-03-24 · draft 21 granitoids were derived from common sources of melting from the...

Draft

Early–Middle Permian postcollisional granitoids in the northern Beishan orogen, NW China: Evidence from U–Pb

ages and Sr–Nd–Hf isotopes

Journal: Canadian Journal of Earth Sciences

Manuscript ID cjes-2019-0088.R2

Manuscript Type: Article

Date Submitted by the Author: 01-Oct-2019

Complete List of Authors: Min, Li; China Geological Survey, Tianjin Center，China Geological Survey; China Geological Survey, North China Center for Geoscience InnovationHoutian, Xin; China Geological Survey, Tianjin Center, China Geological Survey; China Geological Survey, North China Center for Geoscience InnovationBangfang, Ren; China Geological Survey, Tianjin Center, China Geological Survey; China Geological Survey, North China Center for Geoscience InnovationYunwei, Ren; China Geological Survey, Tianjin Center, China Geological Survey; China Geological Survey, North China Center for Geoscience InnovationWengang, Liu; China Geological Survey, Tianjin Center, China Geological Survey; China Geological Survey, North China Center for Geoscience Innovation

Keyword: northern Beishan orogen, Early–Middle Permian, tectonic setting, zircon U–Pb dating, Sr–Nd isotopes, zircon Hf isotopes

Is the invited manuscript for consideration in a Special

Issue? :Not applicable (regular submission)

https://mc06.manuscriptcentral.com/cjes-pubs

Canadian Journal of Earth Sciences

Draft

1 Early–Middle Permian postcollisional granitoids in the northern

2 Beishan orogen, NW China: Evidence from U–Pb ages and Sr–Nd–

3 Hf isotopes

4 Min Li1,2,*, Houtian Xin1,2, Bangfang Ren1,2, Yunwei Ren1,2, and Wengang Liu1,2

5 1Tianjin Center, China Geological Survey, Tianjian, 300170, China

6 2North China Center for Geoscience Innovation, Tianjian, 300170, China

7 Abstract: The geochemistry and Sr–Nd isotope, zircon U–Pb, and zircon Hf isotope

8 compositions are reported for monzogranites and granodiorites from the Hazhu area in

9 the northern Beishan orogen, NW China. Zircon U–Pb dating yields two ages of 270.1

10 ± 1.1 and 277.4 ± 1.2 Ma for the monzogranites and 263.6 ± 1.2 and 262.2 ± 1.1 Ma

11 for the granodiorites. These monzogranites and granodiorites are metaluminous to

12 weakly peraluminous I-type and belong to mid-K calc-alkaline and high-K

13 calc-alkaline series. They exhibit high Mg# values and middle degrees of

14 differentiation (D.I. = 70.7–88.1). They are enriched in large-ion lithophile elements

15 and light rare-earth elements and depleted in high field strength elements. They

16 display high (87Sr/86Sr)i ratios of 0.6995 to 0.7070 and high εNd(t) values of 4.37–5.70

17 with Nd model ages (TDM) of 522–789 Ma, suggesting a juvenile crustal origin.

18 Furthermore, their εHf(t) values are all positive, and Hf isotopic crustal model ages

19 (TC DM = 394–1097 Ma) also indicate a juvenile crustal origin. According to the data

20 obtained in this study and other regional geological data acquired recently, the Hazhu

Page 1 of 56



Draft

21 granitoids were derived from common sources of melting from the Neoproterozoic to

22 Late Paleozoic juvenile crusts. The younger intrusions (granidiorites) are more basic,

23 probably as a result of more juvenile lower crust being melted along with

24 asthenospheric upwelling, which led to the addition of more basic components. These

25 granitoids formed in a postcollisional setting. The tectonic regime transformed from

26 an arc-related compressional setting to postcollisional extension, probably as a result

27 of lithospheric extension and thinning in response to oceanic lithospheric

28 delamination. These granitoids in the northern Beishan orogen were probably

29 emplaced in a postcollisional extensional setting and suggest vertical continental

30 crustal growth in the southern Central Asian Orogenic Belt.

31 Key words：northern Beishan orogen; Early–Middle Permian; tectonic setting;

32 zircon U–Pb dating; Sr–Nd isotopes; zircon Hf isotopes

33 1. Introduction

34 The Central Asian Orogenic Belt (CAOB), located among the Eastern Europe,

35 Siberia, Tarim, and North China plates (Fig. 1a), which evolved from the Late

36 Mesoproterozoic (Kröner et al., 2014), is one of the world’s most significant areas in

37 terms of continental crust growth and transformation in the Phanerozoic (Sengör et

38 al., 1993; Khain et al., 2002; Jahn et al., 2009; Windley et al., 2007; Sun et al., 2008;

39 Xiao et al., 2009,2010; Lei et al., 2011; Wilhem et al., 2012; He et al., 2014; Tian et

40 al., 2015; Zhu et al., 2016). The orogenesis of the CAOB was long-lived, lasting

41 for >800 million years, involving multiple subduction phases and long, continuous

42 accretion and featuring complex accretionary orogenesis and continental growth (Xiao

Page 2 of 56



Draft

43 and Santosh, 2014). The CAOB significantly grew laterally during multiple growth

44 periods in the Paleozoic (Xiao et al., 2008; Xu et al., 2013). The Beishan orogen,

45 situated at the southern margin of the CAOB (Fig. 1b), is a conjunction region of the

46 Kazakhstan plate and North China (Alxa block) and Tarim (Dunhuang block) cratons

47 (Liu et al., 2011; Zhao et al., 2012; Zhang et al., 2012a; Guo et al., 2014; Xu et al.,

48 2014; Zhao et al., 2015). The Beishan orogen is considered to be the eastern extension

49 of the Tianshan orogeny tectonically (Liu and Wang, 1995; Xiao et al., 2010), and it is

50 connected to Tianshan suture zone to the west and to the Soren suture zone to the east

51 (Guo et al., 2012). The Beishan orogen comprises an assemblage of blocks (Su et al.,

52 2012), magmatic arcs, and ophiolitic m é langes formed by subduction–accretion

53 processes of the Paleo-Asian Ocean (Zheng et al., 2014; Cleven, et al., 2015a; Ao et

54 al., 2016).

55 As an important part of the southern margin of the CAOB, granitoids widely

56 developed during the formation of the Beishan orogen in the Paleozoic (Jiang et al.,

57 2006; Su et al., 2011; Zhang et al., 2012b; Li et al., 2013; Jia et al., 2016). Two phases

58 of subduction and collision orogeny occurred in the Beishan area in the Paleozoic.

59 The first phase occurred in the Early Paleozoic from the Middle Cambrian to the Late

60 Silurian (Dai et al., 2003; He et al., 2005). The weighted mean 206Pb–238U age of 533

61 ± 1.7 Ma obtained from a plagiogranite in the Yueyashan–Xichangjing ophiolite

62 indicates that the ocean floor formed during the Early Cambrian (Ao et al., 2012). The

63 Hongliuhe–Niujuanzi–Xichangjing Ocean underwent northward subduction beneath

64 the Mazongshan microcontinent from the Late Ordovician to the Late Silurian (He et

Page 3 of 56



Draft

65 al., 2005; Yang et al., 2013; Cleven et al., 2015b; Song et al., 2016). The ocean closed

66 at the end of the Silurian (He et al., 2005). The second phase occurred in the Late

67 Paleozoic with development of the Hongshishan–Baiheshan Ocean in the Early

68 Carboniferous (He et al., 2005; Wang et al., 2014). After that, the tectonic magmatic

69 evolution is controversial. Considerable research has focused on the southern Beishan

70 orogen in the Late Paleozoic. The Beishan orogen was in a postorogenic stage of the

71 extensional environment in the Late Carboniferous (Feng et al., 2012). From the

72 beginning of the late Early Permian, it progressed to a rift stage during a

73 postcollisional extensional period (Zhang et al., 2011). However, little research has

74 addressed the northern Beishan orogen in the Late Paleozoic, especially in the

75 Permian.

76 In this contribution, we present new geochronological and major and trace

77 element data, as well as Sr–Nd isotopic compositions and zircon Hf isotopic

78 compositions, for the granitoids in the Hazhu area in the northern Beishan orogen.

79 Our aim is to provide further insight into the mechanism of

80 petrogenesis, properties of the magma sources, and tectonic history of the northern

81 Beishan orogen.

82 2. Regional geologic background

83 The tectonic units of the Beishan area are divided into the Tarim plate in the south

84 side and the Kazakhstan plate in the north side (Ao et al., 2012; Yang et al., 2012;

85 Zheng et al., 2012；Tian et al., 2014). A secondary tectonic unit is in the Kazakhstan

86 plate; in order from north to south, this unit comprises the Queershan–Hulishan Early

Page 4 of 56



Draft

87 Paleozoic active continental margin zone, the Hongshishan–Heiyingshan Late

88 Paleozoic active continental margin zone, the Xingxingxia–Mingshui–Hanshan block

89 (Ding et al., 2017), and the Gongpoquan–Dongqiyishan Early Paleozoic active

90 continental margin zone (Yang et al., 2012; Song et al., 2013; Guo et al., 2014; Yu et

91 al., 2016; Wang et al., 2018) (Fig. 1b).

92 The study area, located south of the Hongshishan–Baiheshan–Pengboshan fault,

93 belongs to the Hongshishan–Heiyingshan Late Paleozoic active continental margin

94 zone (Fig. 1b). It mainly comprises Paleozoic strata, including Middle Devonian and

95 Carboniferous strata, and the Carboniferous strata are distributed most widely. The

96 Carboniferous strata include the Lvtiaoshan Formation and the Baishan Formation.

97 The Lvtiaoshan Formation mainly consists of clastic rocks, including sandstones,

98 pebbly sandstones, limestones, and bioclastic limestones. The Baishan Formation

99 mainly consists of felsic volcanic and pyroclastic rocks with eruption–explosion

100 facies, including rhyolite and rhyolitic welded tuff. Additionally, there exist

101 Precambrian overlying sedimentary rocks—the Beishan Rock Group in the

102 southwestern part of the study area.

103 Permian granitoids are situated in the eastern part the study area; these include

104 granodiorites and monzogranites, which form an elliptic complex (Fig. 2). This

105 subrounded pluton, with an outcrop area of 100 km2, invaded the Carboniferous

106 granite and sandstone of the Lvtiaoshan Formation. This resulted in small

107 compressional deformation folds (Fig. 3a) in the sandstone, the fold hinges of which

108 are perpendicular to the compression direction formed by the pluton emplacement.

Page 5 of 56



Draft

109 The monzogranites are located at the edge of the elliptic complex rock, and the

110 granodiorites, which intrude into the monzogranites (Fig. 3b), are located in the center

111 of the elliptic complex rock.

112 And there are many magic microgranular enclaves (MMEs) in the complex; these

113 are spherical (Figs. 3c–3e), with the larger ones being >100 cm in diameter (Fig. 3c).

114 Some of them have fine-grained rims and a chilled border (Fig. 3f). The MMEs have

115 the same plagioclase phenocryst and amphibole phenocryst as the host rock (Figs. 3d–

116 3f), and there are many plagioclase phenocrysts and amphibole phenocrysts in the

117 MMEs (Fig. 3f).

118 The monzogranites are characterized by rapakivi-like texture (Fig. 3g) with

119 massive structure. They are composed of phenocrysts (10%–15%) and matrix (85%–

120 90%), the former consisting of k-feldspar and plagioclase (Fig. 3h) and the latter

121 consisting of k-feldspar, quartz, plagioclase, biotite, and hornblende (Fig. 3h). The

122 rock contains k-feldspar (35%–40%), plagioclase (30%–35%), quartz (20%–25%),

123 biotite (3%–4%), and hornblende (1%–2%).

124 The granodiorites (Fig. 3i) are composed of phenocrysts (10%) and matrix

125 (90%), the former consisting of plagioclase and quartz and the latter consisting of

126 plagioclase, k-feldspar, quartz, biotite, and hornblende. The rock contains plagioclase

127 (50%–55%), k-feldspar (15%–20%), quartz (20%–25%), biotite (1%–2%), and

128 hornblende (3%–4%).

Page 6 of 56



Draft

129 3. Sample analysis method

130 3.1. Zircon U–Pb and Hf isotope analysis

131 Zircons for laser ablation multicollector inductively coupled plasma mass

132 spectrometry (LA-ICP-MS) U–Pb dating were separated from two samples of the

133 monzogranites (02TW19 and 02TW24) and two samples of the granodiorites

134 (02TW31 and 02TW32). Zircon sorting was completed by the Langfang Geological

135 Survey Institute of Hebei Province. The samples were crushed and washed in

136 accordance with the conventional method and separated by magnetic and gravity

137 liquid separation, and then zircon with purity of >99% was selected under a binocular

138 lens. Zircon target making and transmission, reflection, and cathodoluminescence

139 (CL) images were completed with a JXA-8800R electron microprobe at the Tianjin

140 Institute of Geology and Mineral Resources (TIGMR). Zircon U–Pb analyses were

141 conducted by LA-MC-ICP-MS. The laser used was a NEWWAVE 193 nm FX and

142 the mass spectrometer used was Thermo Fisher's NEPTUNE (Geng et al., 2011). The

143 laser spot diameter was 35 m, and helium was used as the carrier gas of the

144 denudation material. The analysis process is described in Yuan et al. (2004) and Liu et

145 al. (2008). The software ICPMSDataCal (Liu et al., 2010) was used to process the

146 final test data offline. Common Pb was corrected by 208Pb following the procedure of

147 Andersen (2002). ISOPLOT 3.0 was used to plot U–Pb age harmonics and calculate

148 the average age weight (Ludwig, 2003).

149 Zircon Hf isotope analysis was conducted in the Isotope Laboratory of TIGMR,

Page 7 of 56



Draft

150 using a NEPTUNE (MC-ICPMS) system at the same oscillation band as but at

151 different location from the U–Pb dating analysis. The measured laser beam diameter

152 was 35 m and the laser pulse frequency was 8–10 Hz. For analysis conditions and

153 processes we refer to Geng et al. (2011). In the analysis process, the value of epsilon

154 Hf(t) is calculated on the basis of the zircon U–Pb age. The decay constant of 176Lu is

155 1.867 × 10−11 year−1 (Soderlund et al., 2004), the ratio of 176Hf/177Hf of chondrite is

156 0.282785, and the ratio of 176Lu/177Hf is 0.0336 (Bouvier et al., 2008). The calculation

157 of deficit mantle model age (TDM) refers to the current deficit mantle 176Hf/177Hf ratio

158 of 0.28325 and 176Lu/177Hf ratio of 0.0384 (Griffin et al., 2000). By assuming that the

159 parent magma of each zircon comes from the average continental crust, the crustal

160 model age (TC DM) of zircon Hf isotopes can be calculated by using the 176Lu/177Hf

161 ratio of 0.015 (Griffin et al., 2002).

162 3.2. Whole-rock geochemistry

163 The whole-rock geochemistry was analyzed at TIGMR. First, the weathering

164 crust was removed from fresh samples and then crushed by a crusher. The crushed

165 samples were ground into powder (>200 mesh) by a ball mill for analysis of major

166 and trace elements. The main elements were determined by X-ray fluorescence

167 spectrometry (XRF). FeO was determined by the volumetric method of hydrofluoric

168 acid–sulfuric acid solution and potassium dichromate titration. The analytical

169 accuracy was better than 2%. The trace elements were measured by ICP-MS, and the

170 analytical accuracy was better than 5%. The detailed analytical procedure followed

Page 8 of 56



Draft

171 that of Gao et al. (2003).

172 3.3. Whole-rock Sr–Nd isotopes

173 Sr–Nd isotope analyses were conducted at TIGMR using a Triton thermal

174 ionizer. The spectral analysis accuracy was better than 0.002%. Sample dissolution

175 was performed using acid digestion (HF + HClO4 + HNO3). Separation of Rb and Sr

176 was done through AG50W × 12 strongly acidic cation exchange resins. Nd was

177 separated and purified by HEHEHP resin (P507) technology. Isotope measurement of

178 the background was conducted within the error range. The results of international

179 standard sample BCR-2 were as follows: 143Nd/144Nd = 0.512630 ± 4 (2σ) and

180 87Sr/86Sr = 0.704985 ± 7 (2σ).

181 4. Results

182 4.1. Zircon U–Pb geochronology

183 The granitoid samples yielded adequate zircons for LA-ICPMS U–Pb dating.

184 The analytical results are listed in Table 1.

185 The zircon grains used for LA-ICP-MS U–Pb analyses of the monzogranite

186 (02TW19 and 02TW24) were mostly euhedral, transparent to translucent, and

187 colorless; they exhibited clear oscillatory zoning with smooth surfaces, were generally

188 120–170 μm in length, and had length/width ratios between 1:1 and 2.5:1. Most

189 zircon grains showed fine prismatic shape with abraded pyramids (Fig. 4). Samples

190 02TW19 and 02TW24 had uranium concentrations ranging from 320 to 1607 and

Page 9 of 56



Draft

191 from 429 to 1958 ppm, respectively, and the Th/U ratio was variable between 0.32

192 and 0.90 and between 0.39 and 0.58, respectively. Zircons of this study are

193 characteristic of magmatic origin and have magmatogenic oscillatory zones.

194 The zircon grains used for LA-ICP-MS U–Pb analyses of the granodiorite

195 (02TW31 and 02TW32) were also mostly euhedral, transparent to translucent, and

196 colorless; they exhibited clear oscillatory zoning with smooth surfaces, were generally

197 100–180 μm in length, and had length/width ratios between 1:1 and 2.5:1. Most

198 zircon grains show fine prismatic shape with abraded pyramids. Compared with

199 zircon grains of the monzogranites, some zircon grains of the granodiorite were

200 subcircular (Fig. 4). Samples 02TW31 and 02TW32 had uranium concentrations

201 ranging from 239 to 1428 ppm and from 267 to 842 ppm, respectively, and their Th/U

202 ratios were variable between 0.44 and 1.52 and between 0.44 and 1.05, respectively.

203 Zircons of this study are characteristic of magmatic origin and have magmatogenic

204 oscillatory zones.

205 Most zircon grain ages of the monzogranite (02TW19) plot on the concordia

206 curve uniformly and are considered to be concordant within error, except for

207 measuring point 19, which falls below the concordia curve in the U–Pb concordia

208 diagram, and its 206Pb/238U value is small, probably resulting from radiogenic Pb loss.

209 Analyses of the data table and concordia plots are reported at the 1σ level and

210 uncertainties in weighted mean ages are quoted at the 95% confidence level. The

211 weighted average 206Pb/238U age of the 23 zircon grains with a confidence of 95% is

212 270.1 ± 1.1 Ma (MSWD = 0.61, n = 23) (Fig. 5).

Page 10 of 56



Draft

213 The 206Pb/238U ages of the zircon grains in the monzogranite (02TW24) exhibit

214 ages mainly of 271–283 Ma. All ages plot on the concordia curve uniformly, and the


216 277.4 ± 1.2 Ma (MSWD = 0.85, n = 24) (Fig. 5).

217 Most zircon grain ages in the granodiorite (02TW31) plot on the concordia curve

218 uniformly. The 206Pb/238U ages of mainly 260–269 Ma are considered to be

219 concordant within error, except for measuring point 18, which falls below the

220 concordia curve in the U–Pb concordia diagram, probably as a result of radiogenic Pb

221 loss. The weighted average 206Pb/238U age of the 23 zircon grains with a confidence of

222 95% is 263.6 ± 1.2 Ma (MSWD = 0.64, n = 23) (Fig. 5).

223 The 206Pb/238U ages of the zircon grains in the granodiorite (02TW32) exhibit

224 ages mainly of 260–265 Ma. All ages plot on the concordia curve uniformly, and the


226 262.2 ± 1.1 Ma (MSWD = 0.31, n = 24) (Fig. 5).

227 In conclusion, zircon ages of 270.1 ± 1.1 and 277.4 ± 1.2 Ma in the late Early

228 Permian can be interpreted as representing the crystallization age of the monzogranite,

229 and zircon ages of 263.6 ± 1.2 and 262.2 ± 1.1 Ma in the late Middle Permian can be

230 interpreted as representing the crystallization age of the granodiorites.

231 4.2. Geochemistry

232 Major and trace element data for 12 representative samples of the monzogranites

233 and granodiorites are presented in Table 2.

Page 11 of 56



Draft

234 Based on the total alkali-silica diagram of Middlemost (1989) (Fig. 6a), these

235 samples plot in the field of granodiorite and granite. Based on the standard ore

236 diagram of Streckeisen (1979), these samples plot in the field of granodiorite and

237 monzogranite (Fig. 6b). These geochemical classification results are confirmed by

238 petrographic studies.

239 The monzogranite and granodiorite (host rock) samples belong to a low-Fe

240 calc-alkaline series (Fig. 6c). The characteristics of major elements can be

241 summarized as follows: (1) SiO2 contents is high (66.12%–73.94%), with

242 differentiation index ranging from 70.70 to 88.07. (2) The A/NK–A/CNK diagram

243 shows that monzogranites and granodiorites range from metaluminous to weakly

244 peraluminous with A/CNK ratios from 0.94 to 1.02 (Fig. 6d). (3) The monzogranites

245 and granodiorites have moderate ALK (Na2O+K2O) contents (6.42%–7.82%) and

246 Na2O contents (3.66%–4.33%). (4) The granodiorite samples exhibit medium-K

247 calc-alkaline properties, while the monzogranites exhibit high-K calc-alkaline

248 properties (Fig. 6e). (5) All samples plot within the magnesian granitoid fields (Fig.

249 6f), and the monzogranite and granodiorite plot within the calc-alkalic field (Fig. 6g)

250 in the classification diagrams of Frost et al. (2001).

251 In the chondrite-normalized rare earth element (REE) diagram (Fig. 7a), the

252 monzogranites and granodiorites have moderately fractionated REE patterns

253 ((La/Yb)N = 5.1–8.9), moderately fractionated light REEs ((La/Sm)N = 3.3–5.0), and

254 weakly fractionated heavy REEs ((Gd/Lu)N = 1.0–1.4). They have low total REE

255 contents (ΣREE = 83.6–129.0 ppm). The granodiorites have slight Eu anomalies

Page 12 of 56



Draft

256 (Eu/Eu* = 0.67–0.92), whereas the monzogranites of this pluton have weaker negative

257 Eu anomalies (Eu/Eu* = 0.44–0.68).

258 In the primitive-mantle-normalized spidergram (Fig. 7b), the monzogranites and

259 granodiorites are all enriched in Rb, Th, U, and light REE and depleted in high field

260 strength elements, such as Ta, Nb, P, and Ti. The monzogranites have low Sr contents

261 (134 × 10−6 to 367 × 10−6) but high Yb contents (1.83–2.31), while the granodiorites

262 contain higher Sr and lower Yb contents than the monzogranites.

263 4.3. Sr–Nd isotopes

264 Sr–Nd isotopic data of the eight granitoids samples are given in Table 3 and are

265 displayed in Fig. 8. All data and parameters are within the normal range and there are

266 no abnormal values. For example, 87Rb/86Sr is not high (<3), so there is no abnormally

267 low Isr value (<0.700), which indicates that the test results have geological

268 significance. In addition, the average fSm/Nd is between −0.6 and −0.2 (Fig. 8a),

269 indicating that the differentiation of the granitoids is not obvious. It can be concluded

270 that Sm–Nd isotopes in the rocks well record the characteristics of their protoliths,

271 which also shows that the model age TDM is effective (Jahn et al., 2000).

272 The four granodiorites samples have positive εNd(t) values (4.37–5.70) and

273 relatively low initial 87Sr/86Sr ratios (0.7021–0.7033), whereas the four monzogranites

274 have positive εNd(t) values (4.52–4.81) and relatively high initial 87Sr/86Sr ratios

275 (0.6995–0.7070). In the diagram of εNd(t) versus (87Sr/86Sr)i, all samples plot in the

276 first and second quadrants (Fig. 8b).

Page 13 of 56



Draft

277 4.4. Zircon Hf isotopes

278 Representative zircons from the paragneiss samples 02TW19.2 and 02TW32.2

279 were chosen for in situ MC-ICP-MS Hf isotope analysis (Table 4). They were taken

280 from the same zircons but different sites as a result of the large size of the

281 laser-ablation pits (Fig. 4). Sixteen zircon grains from the monzogranite (sample

282 02TW19.2) with a weighted mean 206Pb/238U age of 270.1 ± 1.1 Ma have similar Hf

283 isotopic compositions with 176Hf/177Hf ratios of 0.282855–0.283008 (Fig. 9a), εHf(t)

284 values of +8.2 to +14.1 (Fig. 9b), and Hf isotopic crustal model ages (TC DM) of

285 394–772 Ma. Zircon #10 (02TW19.2.10) with a 206Pb/238U age of ~267 Ma has a high

286 176Hf/177Hf ratio of 0.283110, a positive high εHf(t) value of 17.5, and young Hf

287 isotopic crustal model ages (TC DM) of 182 Ma. Sixteen zircon grains from the

288 granodiorite (sample 02TW32.2) with a weighted mean 206Pb/238U age of 262.2 ± 1.1

289 Ma were analyzed: They have variable Hf isotopic compositions, with 176Hf/177Hf

290 ratios of 0.282704–0.283004 (Fig. 9a), εHf(t) values of +3.0 to +13.7 (Fig. 9b), and TC

291 DM of 413–1097 Ma.

292 5. Discussion

293 5.1. Timing of Permian granitic magmatism in the northern Beishan orogen

294 Zircon grains in this study are euhedral and colorless, with typical magmatic

295 oscillatory zoning and high Th/U ratios of 0.32 and 1.11, indicating magmatic origin.

296 Therefore, these ages represent the emplacement ages of the Hazhu Permian

297 granitoids. The results of LA-ICP MS zircon U–Pb dating show that the

Page 14 of 56



Draft

298 monzogranites and granodiorites were crystallized at 262–277 Ma, thus constraining

299 their emplacement age as the Early–Middle Permian. Generally, these results combine

300 with other regional geological data acquired recently indicate that the Permian was an

301 important period of granitic magmatism in the northern Beishan orogen.

302 Numerous research findings have revealed that many Permian granitoids were

303 emplaced in a postorogenic or postcollisional tectonic setting from the eastern

304 Tianshan orogen to the Beishan orogen in NW China (Yuan et al., 2007; Chen et al.,

305 2011; Liu et al., 2012; Zhang et al., 2012; Li et al., 2013). Besides, the emplacement

306 age of the alkaline mafic and felsic magmatism is 280–240 Ma in this regional

307 extensional setting (Pirajno et al., 2010; Song et al., 2011). This age is basically

308 consistent with the zircon U–Pb age (262–277 Ma) of the monzogranites and

309 granodiorites in this study. Generally, research studies on Permian granitoids in the

310 study area have been relatively sparse compared with those on the east Tian orogen

311 and the southern Beishan orogen. Thus, the Permian magmatism, recognized from the

312 northern Beishan orogen in this study, provides further information on Permian

313 magmatism in the northern Beishan orogen and even the CAOB.

314 5.2. Granite types and origin

315 The degree of differentiation of monzogranites and granodiorites are,

316 respectively, medium (D.I. = 82.6–88.1) and low (D.I. = 70.7–79.3). All samples

317 generally plot in I-and S-type granite areas on the FeOT/MgO versus SiO2 diagram

318 (Fig. 6h); however, there are no S-type granite minerals such as muscovite, cordierite,

319 and garnet in the granitoids of this study. On the Ce versus SiO2 diagram, all samples

Page 15 of 56



Draft

320 plot in the I-type granite area. The experimental results show that, in quasi-aluminous

321 and weak peraluminous magma, the solubility of apatite is very low, and it is

322 inversely correlated with SiO2 during magmatic evolution, whereas, in strong

323 peraluminous magma, the solubility of apatite is higher, and the trend is opposite (Zhu

324 et al., 2009). These different behaviors of apatite in I-type and S-type granitoids can

325 be used to distinguish between I-type and S-type granitoids (Li et al., 2007). The data

326 in this study show that all samples exhibit quasi-aluminous characteristics (A/CNK <

327 1.1), and the content of P2O5 is low, decreasing with the increase of SiO2 content,

328 which is consistent with the evolution trend of I-type granite. Therefore, the granitoids

329 of this study exclude the possibility of S-type granites.

330 The zircon saturation temperature (Tzr) of granitoids in this study range from

331 745°C to 782°C (Table 5), which is obviously lower than that of A-type granite,

332 which is >800°C (Liu et al., 2003). Whalen et al. (1987) proposed that AKI

333 ((Na2O+K2O)/Al2O3, molecular number ratio) = 0.85 and ALK (Na2O+K2O) = 8.5%

334 should be the lower limit of A-type granite. The AKI and ALK values of monzonite

335 and granodiorite samples collected in this study do not reach the lower limit of A-type

336 granite, and they are less than the lower limit of AKI (AKI = 1) of alkaline granite.

337 Whalen et al. (1987) also found that A-type granite has the characteristics of low

338 Al and high Ga and Zr. If we take 10000 × Ga/Al = 2.6 as the lower limit value of

339 A-type granite, we find that the 10000 × Ga/Al value of granodiorite and monzonite

340 samples are lower than this value.

341 The contents of Zr, Nb, Ce, and Zr+Nb+Ce+Y are lower than the lower limit

Page 16 of 56



Draft

342 values of A-type granites (Zr = 250×10−6, Nb = 35×10−6, Ce = 148×10−6, and

343 Zr+Nb+Ce+Y = 350×10−6; Whalen, 1987), exhibiting the characteristics of I-type

344 granites (Fig. 6i).

345 5.3. Petrogenesis of the Permian granitoids

346 Geochemical characteristics are primarily controlled by source compositions,

347 physical conditions, partial melting, and fractional crystallization.

348 The Permian granitoids yield similar crystallization ages, uniform zircon Hf

349 isotope compositions, similar Sr–Nd isotope compositions, and coherent

350 major-element composition variations. Thus, the protoliths of the monzogranites and

351 granodiorites most likely share the same genetic origin. Negative correlations of

352 Fe2O3T, MgO, and CaO with respect to SiO2 suggest fractional crystallization of mafic

353 minerals, such as biotite and hornblende. Negative correlations of Fe2O3T, TiO2, and

354 P2O5 with respect to SiO2 suggest fractional crystallization of apatite and ilmenite.

355 K-feldspar phenocrysts formed in the early stage were melted into round spheres

356 by high-temperature mafic magma; afterward, some K-feldspar phenocrysts were

357 surrounded by plagioclase to form rapakivi texture (Fig. 3g). The MMEs exhibit

358 chilled contacts against the host rock. Ellipsoidal, rounded, and lenticular plastic flow

359 patterns show that the MMEs have morphological characteristics of quenched

360 inclusions, which can be distinguished from homologous inclusions and xenoliths,

361 indicating that local magma emplacement is liquid or semisolid. The MMEs in this

362 study are similar to those of the quenched enclaves, which are products of

363 crystallization basic magma with host magma in a plastic state at the same time

364 (Zhang et al., 2012; Shu et al., 2018). This finding provides evidence of the

365 interaction between ferromagnesian magma and felsic magma.

366 Permian granitoids in this study are characterized with positive zircon epsilon Hf

367 values of 3.0 to 14.1 and high 176Hf/177Hf ratios of 0.282855 to 0.283008, which

368 places them between chondrites and depleted-mantle evolution lines (Fig. 9). The

Page 17 of 56



Draft

369 zircon Hf isotopic composition of the granodiorites exhibits obvious heterogeneity

370 with the range of epsilon Hf varying to 10.7 epsilon units. The corresponding Hf

371 isotopic crustal model age (TC DM) is mainly concentrated from 1012 to 394 Ma,

372 which is from the Neoproterozoic to the Devonian. Nd model ages (TDM) are young

373 (0.52–0.79 Ga) for Permian granitoids in this study (Fig. 8c), being similar to

374 Phanerozoic granites in the Central Asia orogen (Kovalenko et al., 1996) and younger

375 than those intruded in microcontinents (Kovalenko et al., 1996; Hong et al., 2000). In

376 the diagram of εNd(t) versus 206Pb/238U age (Fig. 8d), all samples plot between

377 chondrite and depleted mantle, indicating that no Precambrian basement was involved

378 in the formation of granitoids in the study area.

379 By comparison, zircon grains from the Permian granite in the southern Beishan

380 orogen, with a weighted mean 206Pb/238U age of 285 ± 4 Ma, have variable εHf(t)

381 values from weakly negative to weakly positive (−2.7 to +3.2) and TC DM of 0.82–

382 1.04 Ga (Zhang et al., 2012). Moreover, zircon grains from the Silurian granite in the

383 study area, with a weighted mean 206Pb/238U age of 422 ± 2 Ma, have variable εHf(t)

384 values from negative to weakly positive (−5.6 to +3.6) and TC DM of 1.19–1.76 Ga

385 (unpublished). Overall, the Permian granitoids exhibit zircon 176Hf/177Hf and εHf(t)

386 values that are similar to those of the Carboniferous granitoids in this belt, but these

387 values are different from those of Permian and Triassic granitoids in the southern

388 Beishan orogen (Fig. 9). The Permian granitoids exhibit higher εHf(t) values than the

389 Silurian granite in the same area (Fig. 9b). They have positive εHf(t) values between

390 chondrite and primitive mantle, being as high as +14.1, and TC DM of 394–1097 Ma,

391 suggesting source rocks of the Permian granitoids with a characteristic of

392 juvenile crust from the Neoproterozoic to the Late Paleozoic.

393 A great deal of research has shown that the CAOB began to grow and evolve in

394 the Late Mesoproterozoic (Kröner et al., 2014) and is one of the most prominent areas

Page 18 of 56



Draft

395 for the growth and transformation of the Phanerozoic continental crust in the world

396 (Windley et al., 2007; Sun et al., 2008; Xiao et al., 2009, 2010; Wilhem et al., 2012;

397 Li et al., 2018; Li et al., 2019). During the multistage oceanic lithosphere subduction

398 and accretion from the Proterozoic to the Late Paleozoic, large-scale mantle-derived

399 material formed new crust by underplating. Like other parts of the CAOB, the

400 Beishan region underwent large-scale Phanerozoic crustal growth (Jiang and Nie,

401 2006; Mao et al., 2012). At the same time, the Neoproterozoic orogeny extensively

402 existed in the Beishan area, which formed the Neoproterozoic continental crust (Yu et

403 al., 2015; Zong et al., 2017). Besides, isotope studies in the Beishan area indicate

404 significant juvenile input during the Neoproterozoic to Late Paleozoic according to

405 the high epsilon Nd values, zircon epsilon Hf values, young Nd model age, and Hf

406 isotopic crustal model age. Therefore, the Permian granites in the Hazhu area may

407 have been formed by partial melting of the juvenile crust from the Neoproterozoic to

408 Late Carboniferous.

409 In this study, the crust and depleted mantle in the Beishan area are used as

410 mixing endmembers; mantle material involvement ratios during magma formation of

411 Hazhu Permian granodiorites and monzogranites are calculated as 92.0% to 95.3% by

412 simple binary mixing simulation (Table 3). It is further confirmed that the Permian

413 granitoids in the study area were formed by partial melting of juvenile crust

414 containing a numerous mantle-derived components. In the two-component mixing

415 model, the mantle material involvement ratios of the granidiorites (92.8%–95.3%,

416 with an average value of 94.1%) are higher than those of the monzogranites (93.1%–

417 93.7%, with an average value of 93.5%). Meanwhile, the zircon Hf isotopic

418 composition of the granodiorites exhibit obvious heterogeneity with the range of

419 epsilon Hf varying to 10.7 epsilon units, but the range of epsilon Hf of the

420 monzogranites just varies to 5.9 epsilon units. The εNd(t) values of the granidiorites

421 are higher than those of the monzogranites, indicating additional mantle components

422 and juvenile crust. It should be noted that the granidiorites are 10 Ma younger than

423 the monzogranites. Furthermore, the younger intrusion has basic and less evolved

424 composition than the older monzogranite intrusion. Initial 87Sr/86Sr ratios exhibit a

Page 19 of 56



Draft

425 decreasing trend with decreasing SiO2, also indicating additional mantle components

426 and juvenile crust. Although the composite granitoid body has a common source, the

427 variable degree of partial melting during different times means that the monzogranite

428 and granodiorite melts were formed by juvenile crusts of different periods from the

429 Neoproterozoic to the Late Paleozoic. The differences above between the

430 granodiorites and monzogranites demonstrate greater additions of basic components

431 as time progressed, suggesting that more mantle-derived components were added to

432 the magma chamber. Furthermore, the saturation temperature (Tzr) of granitoids in

433 this study was <800°C, suggesting that they emplaced in environments of crustal

434 thickening (Miller et al., 2003) and that during the Early–Middle Permian the tectonic

435 regime probably transformed from compression to extension. In the extensional

436 environment, more and more juvenile lower crust melted and asthenospheric

437 upwelling occurred, which led to the younger intrusion becoming more basic.

438 5.4. Tectonic settings of the Permian granitoids

439 The Permian intrusive rock assemblages are monzogranite, granodiorite, and

440 alkali feldspar granite in the study area. Large-scale crystal caves are developed in the

441 Permian granitoids, indicating an extensional environment. The emplacement age of

442 alkaline mafic felsic magmatism in the regional extensional environment is 280–240

443 Ma (Pirajno et al., 2010; Song et al., 2011; Ma et al., 2016; Zhang et al., 2015; Zhang

444 et al., 2015; Xue et al., 2016), which is basically consistent with the zircon U–Pb age

445 of monzonite and granodiorite (262–277 Ma). Moreover, the Early–Middle Permian

446 olivine gabbro and gabbro diorite are newly defined in the northern Dahongshan area,

447 northwest of the study area. Their geochemical characteristics reflect the

448 characteristics of mantle-derived magma without obvious contamination of crustal

449 materials. This indicates that they formed in the stage of oceanic lithospheric

450 delamination after arc–continent collision. Based on the above facts, it can be

451 concluded that the Permian granitoids formed in the postcollision stage may be

452 closely related to crust–mantle detachment and lithospheric thinning. Although the

453 strong depletion of Nb, Ta, Zr, P, and Ti in the studied granitoids is a typical feature

Page 20 of 56



Draft

454 of subduction-related magmatic rocks, the content of high field strength elements in

455 typical crustal melts is low. This indicates that the depletion of high field strength

456 elements such as Nb, Ta, and Ti inherited the characteristics of source rocks and

457 cannot be used as a sign of subduction-related magmatic rocks.

458 Regionally, the Paleo-Asian Ocean subducted southward during the Early

459 Carboniferous, forming a limited oceanic basin of the Hongshishan–Baiheshan with

460 back-arc cracking origin (Xie et al., 2009; Wang at al., 2014; Li et al., 2018). The Late

461 Carboniferous magmatic arc age on the southern side of the Hongshishan–Baiheshan

462 ophiolite belt is 320 to 300 Ma and its geochemical characteristics exhibit the polarity

463 of the oceanic crust subducting southward. With the southward subduction of the

464 Hongshishan Ocean, a large number of intermediate-acid calc-alkaline magmatic

465 rocks formed in the study area in the Late Carboniferous (Li et al., 2018; Ren et al.,

466 2019); meanwhile, the Paleo-Asian Ocean continued to subduct southward in the Late

467 Carboniferous, forming the Queershan inherited island arc.

468 The Middle–Upper Permian Shuangbaotang Formation strata overlay the

469 Carboniferous Baishan Formation at an unconformity angle in the Shenluotan area.

470 The bottom conglomerates there symbolize the discontinuity of sedimentation at the

471 bottom of the Shuangbaotang Formation strata. The regional arc magmatic events all

472 ended before the Early–Middle Permian, as represented by the sedimentary events of

473 the Shuangbaotang Formation. The isotopic ages of regional alkaline felsic mafic

474 magmatism are 280–240 Ma, which is consistent with the postcollision granitoids

475 under the Permian extensional system in this study. It is presumed that the regional

476 arc–continent collision occurred in the Early Permian, and then the lithospheric

477 extension and thinning caused by oceanic lithospheric delamination resulted in

478 melting of different-period juvenile crusts from the Neoproterozoic to the Late

479 Paleozoic, forming the monzogranites (Fig. 10). As time progressed, more and more

480 juvenile lower crust melted and asthenospheric upwelling occurred, which led to the

481 younger intrusion becoming more basic and to the formation of the granodiorites.

Page 21 of 56



Draft

482 6. Conclusions

483 (1) Zircon U–Pb dating revealed that Early–Middle Permian granitic magmatism

484 occurred at 277–262 Ma in the northern Beishan orogen, NW China. The granitoids

485 exhibit calc-alkaline and high-K calc-alkaline series and are metaluminous to weakly

486 peraluminous I-type.

487 (2) The monzogranites and granodiorites are enriched in large-ion lithophile

488 elements and light REEs and evolved Sr–Nd isotopic compositions, suggesting a

489 juvenile crustal origin. They also exhibit positive εHf(t) values of 3.0 to 14.1 and

490 single-stage Hf model ages of 394 to 797 Ma. Therefore, their source contains

491 juvenile crust from the Neoproterozoic to Late Paleozoic that had positive εHf(t)

492 values at the Early–Middle Permian time.

493 (3) Petrological characteristics and geochemical and isotopic tracing suggest that

494 these granitoids derived from common sources, being melting of Neoproterozoic to

495 Late Paleozoic juvenile crusts. Moreover, the younger intrusions (granidiorites) are

496 more basic, probably the result of more juvenile lower crust being melted along with

497 asthenospheric upwelling, which led to the addition of more basic components.

498 (4) These granitoids formed in a postcollisional setting. The tectonic regime

499 transformed from an arc-related compressional setting to postcollisional extension,

500 probably caused by lithospheric extension and thinning in response to oceanic

501 lithospheric delamination.

Page 22 of 56



Draft

502 Acknowledgments

503 This work was funded by the Geological Survey Project of China (Grant Nos.

504 DD20190371 and DD20190038) and the National Science Foundation of China

505 (Grant No. 41872068).

506 References

507 Andersen, T., 2002. Correction of common lead in U–Pb analyses that do not report

508 204Pb. Chem. Geol. 192, 59–79.

509 Ao, S.J., Xiao, W.J., Han, C.M., Li, X.H., Qu, J.F., Zhang, J.E., Guo, Q.Q., Tian, Z.H.,

510 2012. Cambrian to early Silurian ophiolite and accretionary processes in the

511 Beishan collage, NW China: implications for the architecture of the Southern

512 Altaids. Geological Magazine 149, 106−125. doi:10.1017/S0016756811000884

513 Ao, S.J., Xiao, W.J., Windley, B.F., Mao, Q.G., Han, C.M., Zhang, J.E., Yang, L.K.,

514 Geng, J.Z., 2016. Paleozoic accretionary orogenesis in the eastern Beishan

515 orogen: Constraints from zircon U–Pb and 40Ar/39Ar geochronology. Gondwana

516 30, 224−235.

517 Bouvier, A., Vervoort, J.D., Patchett, P.J., 2008. The Lu–Hf and Sm–Nd isotopic

518 composition of CHUR: Constraints from unequilibrated chondrites and

519 implications for the bulk composition of terrestrial planets. Earth and Planetary

520 Science Letters 273, 48−57.

521 Chen, X.J., Shu, L.S., Santosh, M., 2011. Late Paleozoic post-collisional magmatism

522 in the Eastern Tianshan Belt, Northwest China: new insights from geochemistry,

Page 23 of 56



Draft

523 geochronology and petrology of bimodal volcanic rocks. Lithos 127, 581–598.

524 Cleven, N.R., Lin, S.F., Xiao, W.J., 2015a. The Hongliuhe fold-and-thrust belt:

525 Evidence of terminal collision and suture-reactivation after the Early Permian in

526 the Beishan orogenic collage, Northwest China. Gondwana Research 27,

527 796−810.

528 Cleven, N.R., Lin, S.F., Guilmette, C., Xiao, W.J., Davis, B., 2015b. Petrogenesis and

529 implications for tectonic setting of Cambrian suprasubduction-zone ophiolitic

530 rocks in the central Beishan orogenic collage, Northwest China. Journal of Asian

531 Earth Sciences 113, 369−390.

532 Dai, S., Fang, X.M., Zhang, X., Wang, F.C., Ren. Y.Z., Gao, Z.K., Lei, T.Z., Chen, Y.,

533 2003. Island arc north of the Tarim-SK plate: the geology and geochemistry of

534 Gongpoquan Group. J. Lanzhou Univ. (Natural Sciences) 39, 80−87 (in Chinese

535 with English abstract).

536 Deng, J. F., C. Liu., Feng, Y.F., Xiao, Q.H., Su, S.G., Zhao, G.C., Kong, W.Q., Cao,

537 W.Y., 2010. High Magnesian Andesitic/Dioritic Rocks (HMA) and Magnesian

538 Andesitic/ Dioritic Rocks (MA): Two Igneous Rock Types Related to Oceanic

539 Subduction. Geology in China 37, 1112-1118. (in Chinese with English

540 Abstract).

541 DePaolo, D.J., Linn, A.M., Schubert, G., 1991. The continental crustal age

542 distribution: Methods of determining mantle separation ages from Sm‐Nd

543 isotopic data and application to the southwestern United States. J. Geophys. Res.

544 96, 2071−2088.

Page 24 of 56



Draft

545 Ding, J.X., Han, C.M., Xiao, W.J., Wang, Z.M., Song, D.F., 2017. Geochronology,

546 geochemistry and Sr-Nd isotopes of the granitic rocks associated with tungsten

547 deposits in Beishan district, NW China, Central Asian Orogenic Belt:

548 Petrogenesis, metallogenic and tectonic implications. Ore Geology Reviews

549 2017, 441−462.

550 Feng, J.C., Zhang, W., Wu, T.R., Zheng, R.G., Luo, H.L., He, Y.K., 2012.

551 Geochronology and geochemistry of granite pluton in the north of Qiaowan,

552 Beishan Mountain, Gansu province, China, and its geological significance. Acta

553 Scientiarum Naturalium Universitatis Pekinensis 48, 61−70 (in Chinese with

554 English abstract).

555 Frost, B.R., Barnes, C.G., Collins,W.J., Arculus, R.J., Ellis, D.J., Frost, C.D., 2001. A

556 geochemical classification for granitic rocks. Journal of Petrology 42, 2033–

557 2048.

558 Gao, J.F., Lu, J.J., Lai, M.Y., Lin, Y.P., Pu, W., 2003. Analysis of trace elements in

559 rock samples using HR-ICPMS. J. Nanjing University (Nat. Sci.) 39, 844–850

560 (in Chinese).

561 Geng, J.Z., Li, H.K., Zhang, J., Zhou, H.Y., Li, H.M., 2011. Zircon Hf isotope

562 analysis by means of LA-MC-ICP-MS. Geol. Bull. China 30, 1508−1513 (in

563 Chinese with English abstract).

564 Griffin, W.L., Pearson, N.J., Elusive, E., Jackson, S.E., van Achtenberg, E., O’Reilly,

565 S.Y., She, S.R., 2000. The Hf isotopes composition of carbonic mantle:

566 LAM-MCICPMS analysis of zircon megacrysts in kimberlites. Geochim.

Page 25 of 56



Draft

567 Cosmochim. Acta 64, 133−147.

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

569 Zhou, X.M., 2002. Zircon chemistry and magma mixing, SE China: in-situ

570 analysis of Hf isotopes, Tonglu and Pingtan igneous complexes. Lithos 61,

571 237−269.

572 Guo, Q.Q., Xiao, W.J., Windley, B.F., Mao, Q.G., Han, C.M., Qu, J.F., Ao, S.J., Li,

573 J.L., Song, D.F., Yong, Y., 2012. Provenance and tectonic settings of Permian

574 turbidites from the Beishan Mountains, NW China: Implications for the Late

575 Paleozoic accretionary tectonics of the southern Altaids. Journal of Asian Earth

576 Sciences 49, 54−68.

577 Guo, Q.Q., Xiao, W.J., Hou, Q.L., Xiao, W.J., Hou, Q.L., Windley, B.F., Han, C.M.,

578 Tian, Z.H., Song, D.F., 2014. Construction of Late Devonian Dundunshan arc in

579 the Beishan orogen and its implication for tectonics of southern Central Asian

580 Orogenic Belt. Lithos 184−187, 361−378.

581 He, S.P., Zhou, H.W., Ren, B.C., Yao, W.G., Fu, L.P., 2005. Crustal evolution of

582 Palaeozoic in Beishan area, Gansu and InnerMongolia, China. Northwest

583 Geology 38, 6−15(in Chinese with English abstract).

584 Hong, D.W., Wang, S.G., Xie, X.L., Zhang, J.S., 2000. Genesis of positive εNd(t)

585 granitoids in the Da Xinggan Mts. – Monggolia orogenic belt and growth

586 continental crust. Earth Sci. Front. 7, 441–456 (in Chinese with English abstract).

587 Jahn, B.M., Wu, F.Y., Hong, D.W., 2000. Important crustal growth in the Phanerozoic:

588 Isotopic evidence of granitoids from east-central Asia. India Acad. Sci. (Earth

Page 26 of 56



Draft

589 Planet Sci.) 109, 5–20.

590 Jahn, B.M., Litvinovsky, B.A., Zanvilevich, A.N., Reichow, M., 2009. Peralkaline

591 granitoid magmatism in the Mongolian–Transbaikalian Belt: evolution,

592 petrogenesis and tectonic significance. Lithos 113, 521–539.

593 Jia, Y.Q., Zhao, Z.X., Xu, H., Wang, X.L., Liu, Q., Wang, J.R., 2016. Zircon

594 LA-ICP-MS U-Pb dating of and tectonic setting of rhyolites from Baishan

595 Formation in Fengleishan area of the Beishan orogenic belt. Geol. China 43,

596 91−98 (in Chinese with English abstract).

597 Jiang, S.H., Nie, F.J., 2006. Nd-Isotope constrains on origin of granitoids in Beishan

598 Mountain area. Acta Geol. Sin. 80, 826−842(in Chinese with English abstract).

599 Khain, E.V., Bibikova, E.V., Kröner, A., Zhuaravlev, D.V., Sklyarov, E.V., Fedotova,

600 A.A., Kravchenko-Berezhnoy, I.R., 2002. The most ancient ophiolite of the

601 Central Asian fold belt: U-Pb and Pb-Pb zircon ages for the Dunzhugur Complex,

602 Eastern Sayan, Siberia, and geodynamic implications. Earth and Planetary

603 Science Letters 199, 311~325.

604 Kovalenko, V.I., Yarmolyuk, V.V., Kovach, V.P., Kovach, A.B., Kozakov, I.K.,

605 Sal’nikova, E.B., 1996. Sources of Phanerozoic granitoids in Central Asia:

606 Sm-Nd isotope data. Geochem. Inner. 34, 628−640.

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

608 Seltmann, R., Alexeiev, J.E., Wong, J., Sun, M., Cai, K., Wang, T., Tong, Y.,

609 Wilde, S.A., 2014. Reassessment of continental growth during the accretionary

610 history of the Central Asian Orogenic Belt. Gondwana Research 25, 103–125.

Page 27 of 56



Draft

611 Lei, R.X., Wu, C.Z., Gu, L.X., Zhang, Z.Z., Chi, G.X., Jiang, Y.H., 2011. Zircon U–

612 Pb chronology and Hf isotope of the Xingxingxia granodiorite from the Central

613 Tianshan zone (NW China): Implications for the tectonic evolution of the

614 southern Altaids. Gondwana Research 20, 582–593.

615 Li, M., Ren, B.F., Teng, X.J., Zhang, Y., Duan, X.L., Niu, W.C., Duan, L.F., 2018.

616 Geochemical Characteristics, Zircon U-Pb Age and Hf Isotope and Geological

617 Significance of Granitoid in Beishan Orogenic Belt. Earth Science 43, 4586–

618 4605 (in Chinese with English abstract).

619 Li, M., Xin, H.T., Ren, B.F., Ren, Y.W., Zhang, K., Duan, X.L., Niu, W.C., Duan,

620 L.F., 2019. Petrogenesis and Tectonic Significance of the Late Palaeozoic

621 Granitoids in Hazhu Area, Inner Mongolia. Earth Science 44, 328–343 (in


623 Li, S., Wang, T., Tong, Y., Hong, D.W., OuYang, Z.X., 2009. Identification of the

624 early Devonian Shuangfengshan A-type granites in Liuyuan area of Beishan and

625 its implications to tectonic evolution. Acta Petrologica et Mineralogica 28, 407–


627 Li, S.,Wang, T., Tong, Y., Wang, Y.B., Hong, D.W., OuYang, Z.X., 2011. Zircon

628 U–Pb age, origin and its tectonic significances of Huitongshan Devonian

629 K-feldspar granites from Beishan orogen, NW China. Acta Petrologica Sinica 27,

630 3055–3070 (in Chinese with English abstract).

631 Li, S., Wang, T., Wilde, S.A., Tong, Y., Hong, D.W., Guo, Q.Q., 2012.

632 Geochronology, petrogenesis and tectonic implications of Triassic granitoids

Page 28 of 56



Draft

633 fromBeishan,NWChina. Lithos 134–135, 123–145.

634 Li, S., Wilde, S.A., Wang, T., 2013. Early Permian post-collisional high-K granitoids

635 from Liuyuan area in southern Beishan orogen, NW China: Petrogenesis and

636 tectonic implications. Lithos 179, 99–119.

637 Li, X.H., Li, Z.X., Li, W.X., Liu, Y., Yuan, C., Wei, G.J., Qi, C.S., 2007. U-Pb Zircon,

638 Geochemical and Sr-Nd-Hf Isotopic Constraints on Age and Origin of Jurassic I-

639 and A-Type Granites from Central Guangdong, SE China: a Major Igneous

640 Event in Response to Foundering of a Subducted Flat-Slab? Lithos 96,186−204.

641 Liu, C.S., Chen, X.M., Chen, P.R., Cheng, W.R., Huan, h., 2003. Subdivision,

642 Discrimination Criteria and Genesis for A Type Rock Suites. Geological Journal

643 of China Universities 9, 573–591 (in Chinese with English abstract).

644 Liu, W., Liu, X.J., Xiao, W.J., 2012. Massive granitoid production without massive

645 continental-crust growth in the Chinese Altay: insight into the source rock of

646 granitoids using integrated zircon U–Pb age, Hf–Nd–Sr isotopes and

647 geochemistry. American Journal of Science 312, 629–684.

648 Liu, X.C., Chen, B., Jahn, B.M., Wu, G., Liu, Y.S., 2011. Early Paleozoic (ca. 465

649 Ma) eclogites from Beishan (NW China) and their bearing on the tectonic

650 evolution of the southern Central Asian Orogenic Belt. Journal of Asian Earth

651 Sciences 42, 715−731.

652 Liu, X.Y., Wang, Q., 1995. Tectonics and evolution of the Beishan orogenic belt,

653 West China. Geol. Res 10, 151−165.

654 Liu, Y.S., Hu, Z.C., Gao, S., Günther, Detlef ., Xu, J., Gao, C.G., Chen, H.H., 2008.

Page 29 of 56



Draft

655 In situ analysis of major and trace elements of anhydrous minerals by

656 LA-ICP-MS without applying an internal standard. Chem. Geol. 257, 34−43.

657 doi:10.1016/j.chemgeo.2008.08.004

658 Liu, Y.S., Gao, S., Hu, Z.C., Gao, C.G., Zong, K.Q., Wang, D.B., 2010. Continental

659 and oceanic crust recycling-induced melt-peridotite interactions in the

660 Trans-North China Orogen: U–Pb dating, Hf isotopes and trace elements in

661 zircons of mantle xenoliths. J. Petrol. 51, 537−571.

662 Ludwig, K.R., 2003. ISOPLOT 3.0: A Geochronological Toolkit for Microsoft Excel,

663 Special publication No. 4. Berkeley Geochronology Center, Calif.

664 Ma, J., Lü, X.B., Liu, Y.R., Cao, X.F., Liu, Y.G., Ruan, B.X., Adam, M.M.A., 2016.

665 The impact of early sulfur saturation and calc-crustal contamination on

666 ore-forming process in the Posan mafic–ultramafic complex: Derived from the

667 shallow depleted mantle, Beishan region, NW China. Journal of Asian Earth

668 Sciences 118, 81−94.

669 Maniar, P.D., Piccoli, P.M., 1989. Tectonic discrimination of granitoids. Geological

670 Society of America Bulletin 101, 635−643.

671 Mao, Q.G., Xiao,W.J., Han, C.M., Sun, M., Yuan, C., Zhang, J.E., Ao, S.J., Li, J.L.,

672 2009. Discovery of Middle Silurian adakite granite and its tectonic significance

673 in Liuyuan area, Beishan Moutains, NW China. Acta Petrologica Sinica 26, 584–


675 Mao, Q.G., Xiao,W.J., Fang, T.H.,Wang, J.B., Han, C.M., Sun, M., Yuan, C., 2012.

676 Late Ordovician to early Devonian adakites and Nb-enriched basalts in the

Page 30 of 56



Draft

677 Liuyuan area, Beishan, NW China: implications for early Paleozoic slab-melting

678 and crustal growth in the southern Altaids. Gondwana Research 22, 534–553.

679 Middlemost, E.A.K., 1989. Iron oxidation ratios, norms and the classification of

680 volcanic rocks. Chemical Geology 77, 19–26.

681 Miller, C.F., McDowell, S.M., Mapes, R.W., 2003. Hot and cold granites?

682 Implications of zircon saturation temperatures and preservation of inheritance.

683 Geology 31, 529–532.

684 Naderi, A., Ghasemi, H., Santos, J.F., Rocha, F., Griffin, W.L., Moghadam, H.S.,

685 Papadopoulou, 2018. Petrogenesis and tectonic setting of the Tuyeh-Darvar

686 Granitoid (Northern Iran): Constraints from zircon U-Pb geochronology and

687 Sr-Nd isotope geochemistry. Lithos 318–319, 494–508.

688 Peccerillo, A., Taylor, S.R., 1976. Geochemistry of eocene calc-alkaline volcanic

689 rocks from the Kastamonu area, Northern Turkey. Contributions toMineralogy

690 and Petrology 58, 63–81.

691 Pirajno, F., 2010. Intracontinental strike-slip faults, associated magmatism, mineral

692 systems and mantle dynamics: examples from NW China and Altay-Sayan

693 (Siberia). Journal of Geodynamics 50(3−4), 325−346.

694 Ren, Y.W., Ren, B.F., Niu, W.C., Sun, L.X., Li, M., Zhang, K., Zhang, J.H., Duan,

695 L.F., 2019. Carboniferous Volcanics from the Baishan Formation in the Hazhu

696 Area, Inner Mongolia: Implications for the Late Paleozoic Active Continental

697 Margin Magmatism in the Northern Beishan. Earth Science 44, 312–327 (in


Page 31 of 56



Draft

699 Şengör, A.M.C., Natal’in, B.A., Burtman, V.S., 1993. Evolution of the Altaid tectonic

700 collage and Palaeozoic crustal growth in Eurasia. Nature 364, 209–307.

701 Shu, C.T., Long, X.P., Yin, C.Q., Yuan, C., Wang, Q., He, X.L., Zhao, B.S., Huang,

702 Z.Y., 2018. Continental crust growth induced by slab breakoff in collisional

703 orogens: Evidence from the Eocene Gangdese granitoids and their mafic

704 enclaves, South Tibet. Gondwana Research 64, 35–49.

705 Söderlund, U., Patchett, P.J., Veroort, J.D., Isachsen, C.E., 2004. The 176Lu decay

706 constant determined by Lu-Hf and U-Pb isotope systematics of Percambrian

707 mafic intrusions. Earth and Planetary Science Letters 219, 311−324.

708 Song, D.F., Xiao, W.J., Han, C.M., Li, J.L., Qu, J.F., Guo, Q.Q., Lin, L.N., Wang,

709 Z.M., 2013. Progressive accretionary tectonics of the Beishan orogenic collage,

710 southern Altaids: Insights from zircon U–Pb and Hf isotopic data of high-grade

711 complexes. Precambrian Research 227, 368−388.

712 Song, D.F., Xiao, W.J., Windley, B.F., Han, C.M., Yang, L., 2016. Metamorphic

713 complexes in accretionary orogens: Insights from the Beishan collage, southern

714 Central Asian Orogenic Belt. Tectonophysics 688, 135−147.

715 Song, X.Y., Xie, W., Deng, Y.F., Crawford, A.J., Zheng, W.Q., Zhou, G.F., Deng, G.,

716 Cheng, S.L., Li, J., 2011. Slab break-off and the formation of Permian mafic–

717 ultramafic intrusions in southern margin of Central Asian Orogenic Belt,

718 Xinjiang, NW China. Lithos 127, 128−143.

719 Streckeisen, A., Le Maitre, R.W., 1979. A chemical approximation to the modal

720 QAPF classification of the igneous rocks. N. Jb. Miner. Abh. 136, 169−206.

Page 32 of 56



Draft

721 Su, B.X., Qin, K.Z., Sakyi, P.A., Liu, P.P., Tang, D.M., Malaviarachchi, S.P.K., Xiao,

722 Q.H., Sun, H., Dai, Y.C., Hu, Y., 2011. Geochemistry and geochronology of

723 acidic rocks in the Beishan region, NW China: Petrogenesis and tectonic

724 implications. Journal of Asian Earth Sciences 41, 31−43.

725 Su, B.X., Qin, K.Z., Sun, H., Tang, D.M., Sakyi, P.A., Chu, Z.Y., Liu, P.P., Xiao,

726 W.J., 2012. Subduction-induced mantle heterogeneity beneath Eastern Tianshan

727 and Beishan: Insights from Nd–Sr–Hf–O isotopic mapping of Late Paleozoic

728 mafic–ultramafic complexes. Lithos 134−135, 41−51.

729 Sun,M., Yuan, C., Xiao,W.J., Long, X.P., Xia, X.P., Zhao, G.C., Lin, S.F.,Wu, F.Y.,

730 Kröner, A., 2008. Zircon U–Pb and Hf isotopic study of gneissic rocks fromthe

731 Chinese Altai: progressive accretionary history in the early to middle Paleozoic.

732 Chemical Geology 247, 352–383.

733 Sun, S.S., Mcdonough, W.F., 1989. Chemical and Isotopic Systematics of Oceanic

734 Basalts: Implications for Mantle Composition and Processes. Geological Society

735 London Special Publications 42, 313−345. doi:10.1144/GSL.SP.1989.042.01.19

736 Tian, Z.H., Xiao, W.J., Windley, B.F., Lin, L.N., Han, C.M., Zhang, J.E., Wan, B.,

737 Ao, S.J., Song, D.F., Feng, J.Y., 2014. Structure, age, and tectonic development

738 of the Huoshishan–Niujuanzi ophiolitic mélange, Beishan, southernmost Altaids.

739 Gondwana Research 25, 820−841.

740 Tian, Z.H., Xiao, W.J., Sun, M., Windley, B.F., Glen, R., Han, C.M., Zhang, Z.Y.,

741 Zhang, J.E., Wan, B., Ao, S.J., Song, D.F., 2015. Triassic deformation of

742 Permian Early Triassic arc-related sediments in the Beishan (NWChina): Last

Page 33 of 56



Draft

743 pulse of the accretionary orogenesis in the southernmost Altaids. Tectonophysics

744 662, 363–384.

745 Wang, G.Q., Li, XM., Xu, X.Y., Yu, J.Y., Wu, Peng., 2014. Ziron U-Pb chronological

746 study of the Hongshishan ophiolite in the Beishan area and their tectonic

747 significance. Acta Petrologica Sinica 30, 1685−1694(in Chinese with English

748 abstract).

749 Wang, T., Li, W.P., Li, J.B., Hong, D.W., Tong, Y., Li, S., 2008. Increase of junenal

750 mantle-drived composition from syn-orogenic to post-orogenic granites of the

751 east part of the eastern Tianshan (China) and implications for continental vertical

752 growth: Sr and Nd isotopic evidence. Acta Pertrologica Sinica 24, 762−772(in


754 Wang, X.Y., Yuan, C., Zhang, Y.Y., Long, X.P., Sun, M., Wang, L.X., Soldner, J.,

755 Lin, Z.F., 2018. S-type granite from the Gongpoquan arc in the Beishan

756 Orogenic Collage, southern Altaids: Implications for the tectonic transition.

757 Journal of Asian Earth Sciences 153, 206−222.

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

759 Characteristics, Discrimination and Petrogenesis. Contrib Mineral Petrol 95,

760 407–419.

761 Wilhem, C., Windley, B.F., Stampfli, G.M., 2012. The Altaids of Central Asia: a

762 tectonic and evolutionary innovative review. Earth-Science Reviews 113, 303–

763 341.

764 Windley, B.F., Alexeiev, D., Xiao, W., Kröner, A., Badarch, G., 2007. Tectonic

Page 34 of 56



Draft

765 models for accretion of the Central Asian Orogenic Belt. Journal of the

766 Geological Society of London 164, 31–47.

767 Wu, F.Y., Jahn, B.M., Wilde, S.A., Lo, C.H., Yui, T.F., Lin, Q., Ge, W.C., Sun, D.Y.,

768 2003. Highly fractionated I-type granites in NE China (I): geochronology and

769 petrogenesis. Lithos 66, 241−273.

770 Xiao,W.J., Han, C.M., Yuan, C., Sun, M., Lin, S.F., Chen, H.L., Li, Z.L., Li, J.L., Sun,

771 S., 2008. Middle Cambrian to Permian subduction-related accretionary

772 orogenesis of North Xinjiang,NW China: implications for the tectonic evolution

773 of Central Asia. Journal of Asian Earth Sciences 32, 102–117.

774 http://dx.doi.org/10.1016/j.jseas.2007.1010.100

775 Xiao,W.J.,Windley, B.F., Yuan, C., Sun,M., Han, C.M., Lin, S.F., Chen, H.L., Yan,

776 Q.R., Liu, D.Y., Qin, K.Z., Li, J.L., Sun, S., 2009. Paleozoic multiple

777 subduction–accretion processes of the southern Altaids. American Journal of

778 Science 309, 221–270.

779 Xiao,W.J., Mao, Q.G.,Windley, B.F., Han, C.M., Qu, J.F., Zhang, J.E., Ao, S.J., Guo,

780 Q.Q., Cleven, N.R., Lin, S.F., Shan, Y.H., Li, J.L., 2010. Paleozoic multiple

781 accretionary and collisional processes of the Beishan orogenic collage. American

782 Journal of Science 310, 1553–1594.

783 Xiao, W.J., Santosh, M., 2014. The western Central Asian Orogenic Belt: A window

784 to accretionary orogenesis and continental growth. Gondwana Research 25,

785 1429–1444.

786 Xie, C.L., Yang, J.G., Wang, L.S., Wang, Y.X., Wang, J.P., 2009. Disscussion on the

Page 35 of 56



Draft

787 Location of Paleozoic Island Arc Zone on the South Margin of Paleo-Asian

788 Ocean in the Beishan Area of Gansu Province. Acta Geol. Sinica 83,

789 1584−1600(in Chinese with English abstract).

790 Xu, Q.Q., Ji, J.Q., Zhao, L., Gong, J.F., Zhou, J., He, G.Q., Zhong, D.L.,Wang, J.D.,

791 Griffiths, L., 2013. Tectonic evolution and continental crust growth of Northern

792 Xinjiang in northwestern China: remnant ocean model. Earth-Science Reviews

793 126, 178–205. http://dx.doi.org/10.1016/j.earscirev.2013.08.005.

794 Xu, X.W., Li, X.H., Jiang, N., Li, Q.L., Qu, X., Yang, Y.H., Zhou, G.Z., Dong, L.H.,

795 2014. Basement nature and origin of the Junggar terrane:New zircon U-Pb-Hf

796 isotope evidence from Paleozoic rocks and their enclaves. Gondwana Research

797 28, 288−310.

798 Xue, S.C., Li, C.S., Qin, K.Z., Tang, D.M., 2016. A non-plume model for the Permian

799 protracted (266–286 Ma) basaltic magmatism in the Beishan–Tianshan region,

800 Xinjiang,Western China. Lithos 256–257,243–249.

801 Yang, H.Q., Zhao, G.B., Li, Y., Jiang, H.B., Tan, W.J., Ren, H.N., Wang, X.A.,

802 Xiong, Z.Y., Zhang, X.P., 2012. The relationship between Paleozoic tectonic

803 setting and mineralization in Xinjiang-Gansu-Inner Mongolia juncture area.

804 Geological Bulletin of China 31, 413−421 (in Chinese with English abstract).

805 Yang, Y.Q., Lü, B., Meng, G.X., Yan, J.Y., Zhao, J.H., Wang, S.G., Jia, L.L., Han,

806 J.G., 2013. Geochemistry, SHRIMP Zircon U-Pb Dating and Formation

807 Environment of Dongqiyishan Granite, Inner Mongolia. Acta Geoscientica

808 Sinica 34, 163−175(in Chinese with English abstract).

Page 36 of 56



Draft

809 Yu, J.Y., Guo, L., Li, J.X., Li, Y.G., Smithies, R.H., Wingate, M.T.D., Meng, Y.,

810 Chen, S.F., 2016. The petrogenesis of sodic granites in the Niujuanzi area and

811 constraints on the Paleozoic tectonic evolution of the Beishan region, NW China.

812 Lithos 255−257, 250−268.

813 Yuan, C., Sun, M., Xiao, W.J., Li, X.H., Chen, H.L., Lin, S.F., Xia, X.P., Long, X.P.,

814 2007. Accretionary orogenesis of the Chinese Altai: insights from the Paleozoic

815 granitoids. Chemical Geology 242, 22–39.

816 Yuan, H.L., Gao, S., Liu, X.M., Li, H.M., Günther, Detlef., Wu, F.Y., 2004. Accurate

817 U-Pb age and trace element determinations of Zircon by laser

818 ablation-inductively coupled plasma-mass spectrometry. Geostandards and

819 Geoanalytical Research 28, 353−370.

820 Yuan, Y., Zong, K.Q., He, Z.Y., Klemd, R., Liu, Y.S., Hu, Z.C., Guo, J.L., Zhang,

821 Z.M., 2015. Geochemical and geochronological evidence for a former

822 earlyNeoproterozoic microcontinent in the South Beishan Orogenic

823 Belt,southernmost Central Asian Orogenic Belt. Precambrian Research 266,

824 409−424.

825 Zhang, W., Feng, J.C., Zheng, R.G., Wu, T.R., Luo, H.L., He, Y.K., Jing, X., 2011.

826 LA-ICPMS zircon U–Pb ages of the granites from the south of Yin’aoxia and

827 their tectonic significances. Acta Petrologica Sinica 27, 1649−1661 (in Chinese

828 with English abstract).

829 Zhang, W., Pease, V., Wu, T., Zheng, R.G., Feng, J., He, Y.K., Luo, H.L., Xu, C.,

830 2012a. Discovery of an adakite-like pluton near Dongqiyishan (Beishan, NW

Page 37 of 56



Draft

831 China) —Its age and tectonic significance. Lithos 142−143, 148−160.

832 Zhang, W., Wu, T.R., Zheng, R.G., Feng, J.C., Luo, H.L., He, Y.K., Xu, C., 2012b.

833 Post-collisional Southeastern Beishan granites: Geochemistry,

834 geochronology,Sr−Nd−Hf isotopes and their implications for tectonic evolution.

835 Journal of Asian Earth Sciences 58, 51−63.

836 Zhang, W., Pease, V., Meng, Q.P., Zheng, R.G., Thomsen, T.B.,

837 Wohlgemuth-Ueberwasser, C., Wu, T.R., 2015. Timing, petrogenesis, and

838 setting of granites from the southern Beishan late Palaeozoic granitic belt,

839 Northwest China and implications for their tectonic evolution. International

840 Geology Review 57, 1975−1991.

841 Zhang, Y.Y., Yuan, C., Sun, M., Long, X.P., Xia, X.P., Wang, X.Y., Huang, Z.Y.,

842 2015. Permian doleritic dikes in the Beishan Orogenic Belt, NW China:

843 Asthenosphere–lithosphere interaction in response to slab break-off. Lithos 233,

844 174−192.

845 Zhao, J., Wang, W.L., Dong, L.H., Yang, W.Z., Cheng, Q., 2012. Application of

846 geochemical anomaly identification methods in mapping of intermediate and

847 felsic igneous rocks in eastern Tianshan, China. Journal of Geochemical

848 Exploration 122, 81−89.

849 Zhao, Z.Y., Zhang, Z.C., Santosh, M., Huang, H., Cheng, Z.Y., Ye, J.C., 2015. Early

850 Paleozoic magmatic record from the northern margin of the Tarim Craton:

851 Further insights on the evolution of the Central Asian Orogenic Belt. Gondwana

852 Research 28, 328−347.

Page 38 of 56



Draft

853 Zheng, R.G., Wu, T.R., Zhang, W., Feng, J.C., 2012. The tectonic setting and

854 geochemical characteristics of the Yueyashan-Xichangjing ophiolite in beishan

855 area. Acta Geologica Sinica 86, 961−971 (in Chinese with English abstract).

856 Zheng, R.G., Wu, T.R., Zhang, W., Meng, Q.P., Zhang, Z.Y., 2014. Geochronology

857 and geochemistry of late Paleozoic magmatic rocks in the Yinwaxia area,

858 Beishan: Implications for rift magmatism in the southern Central Asian Orogenic

859 Belt. Journal of Asian Earth Sciences 91, 39−55.

860 Zhu, D.C., Mo, X.X., Wang, L.Q., Zhao, Z.D., Niu, Y.L., Zhou, C.Y., Yang, Y.H.,

861 2009. Petrogenesis of highly fractionated I-type granites in the Chayu area of

862 eastern Gangdese, Tibet: Constraints from zircon U-Pb geochronology,

863 geochemistry and Sr-Nd-Hf isotopes. Sci China Ser D-Earth Sci 39, 833−848 (in

864 Chinese). doi: 10.1007/s11430-009-0132-x

865 Zhu, J., Lv, X.B., Peng, S.G., 2016. U-Pb zircon geochronology, geochemistry and

866 tectonic implications of the early Devonian granitoids in the Liuyuan area,

867 Beishan, NW China. Geosciences Journal 20, 609−625.

868 Zong, K.Q., Klemd, R., Yuan, Y., He, Z.Y., Guo, J.L., Shi, X.L., Liu, Y.S., Hu, Z.C.,

869 Zhang, Z.M., 2017. The assembly of Rodinia: The correlation of early

870 Neoproterozoic (ca.900 Ma) high-grade metamorphism and continental arc

871 formation in the southern Beishan Orogen, southern Central Asian Orogenic Belt

872 (CAOB). Precambrian Research 290, 32−48.

Page 39 of 56



Draft

A list of figure captions Fig. 1. Simplified tectonic location map for the Beishan orogeny (modified after Yang et al., 2012;

Li et al., 2013)

Fig. 2. Geological sketch map of Hazhu area in Ejina banner

Fig. 3. Field potos and photomicrographs of the granitoids in Hazhu area

Fig. 4. CL image and dating of zircons for the monzogranite and granodiorite（yellow circle

represent U-Pb measure point and blue circle represent Hf isotope measure point）

Fig. 5. Zircon LA-MC-ICP-MS U-Pb concordia diagram of the monzogranite and granodiorite

Fig. 6. Major element diagrams

Fig. 7. (a) Chondrite-normalized rare earth element patterns and (b) primitive mantle-normalized

trace element spider diagrams.

Fig. 8 . (a) fSm/Nd vs. TDM diagram for the granitoids, (b) εNd(t) vs. (87Sr/86Sr)i diagram,

(c) εNd(t) vs. TDM diagram, (d) εNd(t) vs. intrusive U–Pb Age diagram

Fig. 9 . (a) 176Hf/177Hf vs. intrusive U–Pb age diagram and (b) εHf(t) vs. intrusive U–Pb age

diagram

Fig. 10. Schematic diagram showing the petrogenetic model for the Permian granitoids in northern

Beishan orogen

Page 40 of 56



Draft

C A O B

Siberia

Craton

Eas

tE

uope

anC

rato

n

a

Tianshan solonker

NorthChinaTarim

TETHYSIDES

Fig.1b

Queershan arc

Baiyushan-Huaniushan arc

Aqishan-Zhangfangshan rift zone

Heiyingshan arc Gongpoquan arcXingxingxia-Hanshan Block

National border Fault

b

Dunhuang Blcok

Dunhuang Blcok

NiujuanziShibanjin

Heiyingshan

Aqishan

Hanshan

Xichangjin

0 40 80 120 160kmMongolia

40°

40°

41°

42°

42°

00′

40′

20′

00′

40′

93° 94° 95° 96° 97° 98° 99° 100°

Hongliuyuan

Hongliuhe

Huaniushan

Fig.2

N

Fig. 1. Simplified tectonic location map for the Beishan orogeny (modified after Yang et al., 2012; Li et al., 2013)

Beishan Rock Group

Carboniferous granite

Devonian

Permian granodiorite

Carboniferous

Permian monzogranite

Carboniferous andersite

Cretaceous Quaternary sample location

Carboniferous rhyolite

0 1 2 km

N

42°15′

98°30′

42°00′

99°00′

42°00′

98°30′

Fig. 2. Geological sketch map of Hazhu area in Ejina banner

Page 41 of 56



Draft g

200μm

1i

Qtz

Hbl

Bt

Pl

200μm

h

QtzPl

Hbl

Bt

Kfs

Pl

Hbl

porphyritic granodiorite

porphyritic monzogranite

b

mafic enclave

porphyritic monzogranite

e

plagioclase phanerocryst

d


a

folds in country rock

f


amphibole phanerocryst

rapakivi-like texture

c

Fig. 3. Field potos and photomicrographs of the granitoids in Hazhu areaa Folds in country rock; b Intrusion relationship; c MME in monzogranite; d – Plageioclase phanerocryst in monzogranite; e

Plageioclase phanerocryst in granodiorite; f Plageioclase and amphibole phanerocryst in granodiorite and MME; g Rapakivi-like texture; h Photomicrographs of monzogranite; i Photomicrographs of granodiorite. Mineral abbreviation: Qtz, quartz; Pl,

plagioclase; Bt, biotite; Hbl, hornblende; Kfs, K-feldspar.

Page 42 of 56



Draft

275±3 275±3278±3

278±3277±3

277±3

278±3

277±3277±3

279±3

279±3279±3

276±3

278±3242322

1916

1413

121098631

271±3

270±3

271±3

270±3

269±3271±3

269±3266±3

271±3

21

4

36

4

7

596

10 7

148 1711

271±3

2113

269±3

20

14

2315 24

16

265±3 264±3262±3

262±3

262±3

263±3 265±3

264±3263±4

263±3

264±3

265±3 263±3

264±3

1 3 45 6 7 10

13 14 15

17 2223 24

261±3

261±3 260±3261±3Ma 265±3

262±3264±3

261±3

263±3

263±3262±3

263±3

263±3 261±3

31 4

2 7 3 8410

5 12 613 7

148

159

1610 18 12 2214

23 1524 16

275±3

02TW19

02TW24

02TW31

02TW32

100μm

Fig. 4. CL image and dating of zircons for the monzogranite and granodiorite（yellow circle represent U-Pb measure point and blue circle represent Hf isotope measure point）

Page 43 of 56



Draft250

254

258

262

266

270

274

278

0.0395

0.0405

0.0415

0.0425

0.0435

0.0445

0.25 0.27 0.29 0.31 0.33 0.35207

Pb/235

U

254258

262

266

270

274

250

254

258

262

266

270

274

0.0395

0.0405

0.0415

0.0425

0.0435

0.26 0.28 0.30 0.32

254

258

262

266

270

258

262

266

270

274

278

282

286

0.0405

0.0415

0.0425

0.0435

0.0445

0.0455

0.28 0.29 0.30 0.31 0.32 0.33

20

6 Pb

/23

8 U

260

268

276

284

(a)02TW19

270.1±1.1MaMSWD=0.61,n=23

260

264

268

272

276

280

284

288

292

296

0.041

0.042

0.043

0.044

0.045

0.046

0.047

0.28 0.29 0.30 0.31 0.32 0.33 0.34

264

272

280

288

(b)02TW24

277.4±1.2MaMSWD=0.85,n=24

(c)02TW31 263.6±1.2MaMSWD=0.64,n=23

20

6 Pb

/23

8 U

20

6 Pb

/23

8 U

(d)02TW32

262.2±1.1MaMSWD=0.31,n=24

20

6 Pb

/23

8 U

207Pb/

235U

Fig. 5. Zircon LA-MC-ICP-MS U-Pb concordia diagram of the monzogranite and granodiorite

Page 44 of 56



Draft

( )

0

1

2

3

4

5

6

7

45 50 55 60 65 70 75 80

TF

eO

/Mg

O

SiO2

strong CA series

CA

LF-CA

TH

0

1

2

3

0.5 0.7 0.9 1.1 1.3 1.5 1.7 1.9

A/N

K

A/CNK

CCG

CAG

IAG

RAG

POG

I-Stype( )d

Peraluminous

Peralkaline

Metaluminous

0.4

0.5

0.6

0.7

0.8

0.9

1.0

1.1

50 55 60 65 70 75 80

TT

FeO

/(F

eO+

Mg

O)

SiO2

Caledonian post- collisiona plutons (Frost et al.,2001)

( )f

Ferroan

Magnesian

-6

-4

-2

0

2

4

6

8

10

12

50 55 60 65 70 75 80

Na

O+

KO

22

-CaO

SiO2

(g)

Caledonian post- collisiona plutons (Frost et al.,2001)

alkalic

alkali-calcic

calc-alkalic

calcic

0

1

2

3

4

5

6

7

40 50 60 70 80K

O2

SiO2

Low-K

Calc-alkaline

High-K

Shoshonitic

(e)

5

15

25

35

45

0 10 20 30 40 50 60 70 80

Q'

ANOR

(b)

monzogranite

granodiorite

0

3

6

9

12

15

18

30 40 50 60 70 80 90

Na

O+

KO

22

SiO2

Ir

(a)

granite

granodiorite

SiO2

0.1

1

10

100

65 70 75 80

TF

eO

/Mg

O A

I&S

(h)

Zr+Nb+Ce+Y10 100 1000 10000

1

10

100

(Na

O+

KO

)/C

aO2

2

(i)

A

FG

OGT

cmonzogranitegranodiorite

Fig. 6. Major element diagrams. (a) Total alkalis vs. SiO2 (TAS) diagram (after Middlemost, 1989), (b)Q’ vs. ANOR standard ore diagram (modified after Streckeisen, 1979), (c) total FeO /MgO vs. SiO2 (after

Deng et al., 2010), (d) A/NK vs. A/CNK diagram (after Maniar and Piccoli, 1989), (e)K2O vs. SiO2 diagram (after Peccerillo and Taylor, 1976), (f) total FeO/(total FeO + MgO) vs. SiO2

diagram (after Frost et al., 2001), (g) Na2O + K2O–CaO vs. SiO2 diagram (after Frost et al., 2001), (h) total FeO/MgO vs. SiO2 diagram, (i) (Na2O + K2O)/CaO vs. (Zr + Nb + Ce + Y) diagram (Whalen et al., 1987).

Total FeO (FeOT) = FeO + 0.9 Fe2O3, A/CNK = mol Al2O3/(Na2O + K2O + CaO), A/NK = mol Al2O3/(Na2O + K2O), FG: fractionated granites; OGT: unfractionated M-, I- and S-type granites

Page 45 of 56



Draft

0.1

1

10

100

1000

Ro

ck/C

ho

nd

rite

0.1

1

10

100

1000

Ro

ck/P

rim

itiv

e M

antl

emonzogranitegranodiorite

(a) (b)

La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Rb BaTh U Nb Ta K La Ce Sr P Nd Zr Hf SmEu Ti Tb Y Yb Lu

Fig. 7. (a) Chondrite-normalized rare earth element patterns and (b) primitive mantle-normalized trace element spider diagrams.The values of chondrite and primitive mantle are from Sun and Mcdonough (1989).

-0.8

-0.6

-0.4

-0.2

0.0

0.2

0.0 0.2 0.4 0.6 0.8

f Sm

/Nd

T (Ga)DM

(a)

(87Sr/86Sr) I

0.690 0.700 0.710 0.720 0.730 0.740

ε Nd

15

10

5

0

-5

-10

-15

-20

(b)

Eastern Tian shan andSouthern Beishan intrusions

East Tianpost orogenic granites

mantle array

granodiorites

monzogranitesEMⅠ

EMⅡ

-20

-15

-10

-5

0

5

10

15

0.0 0.1 0.2 0.3 0.4 0.5

Age (Ga)

ε Nd

-20

-15

-10

-5

0

5

10

0.0 0.5 1.0 1.5 2.0 2.5 3.0

ε Nd

T (Ga)DM

Hercyniangranites(France)

Himalayagranite

CHUR

Archaean Crust

Early-Middle Proterozoic Crust

CHUR

Depleted Mantle

c( ) (d)

granodiorite

monzogranite

Central Asia granitesmicrocontinents

Data: Kovalenko et al.(1996)

granodiorite

monzogranite

Fig. 8 . (a) fSm/Nd vs. TDM diagram for the granitoids, (b) εNd(t) vs. (87Sr/86Sr)i diagram, (c) εNd(t) vs. TDM diagram, (d) εNd(t) vs. intrusive U–Pb Age diagram. Fields dapted from Naderi

et al. (2018), and reference compositions dapted from Wang et al. (2008)

Page 46 of 56



Draft

-20

-15

-10

-5

0

5

10

15

20

200 250 300 350 400 450 500

ε(t

)H

f

Age

Depleted mantle

CHUR

(b)

Triassicgranitoids

Pemian granitoids in southern Beishan

Carboniferous-Pemian granitoids in northern Beishan

Silurian granitoidsin northern Beishan

0.2820

0.2825

0.2830

0.2835

200 250 300 350 400 450 500

17

61

77

Hf/

Hf

Age

Depleted mantle

CHUR

Lower crust

(a)

Silurian granitoidsin northern Beishan

Carboniferous-Pemian granitoids in northern Beishan

granodiorite

monzogranite

Fig. 9 . (a) 176Hf/177Hf vs. intrusive U–Pb age diagram and (b) εHf(t) vs. intrusive U–Pb age diagram. Data for Siluriangranitoids and Triassic granitoids in the centralmassif and Permian granitoids in the southernmassif are from Li et al. (2009, 2011,

2012), Mao et al. (2009) and Zhang et al. (2012).

Lithosp

heric

man

tle

Lithospheric mantle

breakoff slab

Baiheshan accretio

nary complex

Baishan arc

Continen

tal c

rust

junenile crustal MASH zone

Carboniferousgranitoids Permian granitoids

Extension

Upwelling asthenosphere

Continental crust

CarboniferousBaishan Formation

Permian Shuangbaotang Formation

unconformity

N S

W

E

Permian (277-262Ma)

Oceanic crust Asth

enosp

here m

antle

Asthenosphere mantle

Fig. 10. Schematic diagram showing the petrogenetic model for the Permian granitoids in northern Beishan orogen

Page 47 of 56



DELL

打字机文本

Draft

Table 1

Table 1 Zircon LA-MC-ICP-MS U-Pb dating result of the monzogranites (02TW19.2 and 02TW24.1) and granodiorites (02TW31.1 and 02TW32.2)Spot No. 含量(×10-6) Isotopic ratios Apparent age (Ma)

02TW19.2 Pb U 206Pb/238U 1σ 207Pb/235U 1σ 207Pb/206Pb 1σ 208Pb/232Th 1σ 232Th/238U 1σ 206Pb/238U 1σ 207Pb/235U 1σ 207Pb/206Pb 1σ

1 36 839 0.0428 0.0004 0.3099 0.0044 0.0525 0.0006 0.0144 0.0001 0.3476 0.0006 270 3 274 4 308 28

2 51 1150 0.0429 0.0004 0.3088 0.0053 0.0522 0.0007 0.0158 0.0002 0.3849 0.0010 271 3 273 5 294 31

3 30 565 0.0438 0.0004 0.3111 0.0047 0.0516 0.0007 0.0305 0.0001 0.5041 0.0013 276 3 275 4 266 30

4 46 1043 0.0428 0.0004 0.3068 0.0044 0.0520 0.0006 0.0156 0.0001 0.3939 0.0005 270 3 272 4 286 27

5 31 656 0.0425 0.0004 0.3074 0.0043 0.0524 0.0007 0.0208 0.0001 0.4426 0.0006 268 3 272 4 304 28

6 50 1132 0.0429 0.0005 0.3091 0.0043 0.0523 0.0006 0.0151 0.0001 0.3974 0.0009 271 3 273 4 296 27

7 51 1173 0.0427 0.0004 0.3088 0.0041 0.0524 0.0006 0.0156 0.0000 0.3219 0.0013 270 3 273 4 303 27

8 28 627 0.0428 0.0004 0.3066 0.0044 0.0519 0.0007 0.0160 0.0001 0.3818 0.0011 270 3 272 4 283 31

9 43 937 0.0426 0.0004 0.3070 0.0046 0.0523 0.0007 0.0160 0.0001 0.4803 0.0006 269 3 272 4 298 29

10 48 1065 0.0429 0.0004 0.3074 0.0041 0.0520 0.0006 0.0141 0.0000 0.4647 0.0010 271 3 272 4 285 27

11 27 613 0.0427 0.0004 0.3084 0.0046 0.0524 0.0007 0.0142 0.0001 0.4432 0.0032 270 3 273 4 302 30

12 30 669 0.0429 0.0004 0.3079 0.0060 0.0521 0.0009 0.0134 0.0002 0.4666 0.0008 271 3 273 5 288 41

13 27 613 0.0429 0.0004 0.3084 0.0044 0.0522 0.0007 0.0126 0.0000 0.4713 0.0015 270 3 273 4 294 30

14 40 826 0.0436 0.0004 0.3125 0.0050 0.0520 0.0008 0.0114 0.0000 0.9016 0.0010 275 3 276 4 284 34

15 14 320 0.0427 0.0004 0.3035 0.0079 0.0516 0.0014 0.0094 0.0001 0.7555 0.0090 269 3 269 7 268 63

16 30 699 0.0423 0.0004 0.3038 0.0050 0.0521 0.0008 0.0118 0.0001 0.4785 0.0015 267 3 269 4 288 35

17 23 527 0.0425 0.0004 0.3051 0.0062 0.0520 0.0010 0.0104 0.0001 0.5838 0.0012 269 3 270 5 287 43

18 26 607 0.0427 0.0004 0.3051 0.0071 0.0518 0.0011 0.0133 0.0002 0.4081 0.0010 269 3 270 6 278 49

19 32 805 0.0372 0.0004 0.3725 0.0052 0.0726 0.0009 0.0141 0.0001 0.4049 0.0008 235 2 322 5 1004 25

20 28 643 0.0427 0.0004 0.3088 0.0048 0.0525 0.0007 0.0126 0.0001 0.4182 0.0011 269 3 273 4 306 32

21 25 566 0.0429 0.0004 0.3053 0.0045 0.0516 0.0007 0.0124 0.0001 0.3971 0.0003 271 3 271 4 267 31

22 30 695 0.0429 0.0004 0.3042 0.0051 0.0515 0.0008 0.0123 0.0001 0.4183 0.0006 270 3 270 5 263 36

23 22 507 0.0421 0.0004 0.3039 0.0069 0.0523 0.0011 0.0136 0.0001 0.4228 0.0003 266 3 269 6 300 49

24 77 1607 0.0429 0.0004 0.3077 0.0042 0.0521 0.0006 0.0136 0.0001 0.7649 0.0030 271 3 272 4 288 27

Spot No. 含量(×10-6) Isotopic ratios Apparent age (Ma)

Page 48 of 56



Draft


1 45 964 0.0436 0.0004 0.3134 0.0048 0.0521 0.0007 0.0172 0.0001 0.4716 0.0002 275 3 277 4 290 29

2 28 590 0.0443 0.0004 0.3178 0.0055 0.0520 0.0008 0.0160 0.0001 0.4637 0.0015 280 3 280 5 286 37

3 29 629 0.0437 0.0004 0.3129 0.0046 0.0520 0.0007 0.0156 0.0000 0.4769 0.0015 275 3 276 4 285 30

4 40 848 0.0434 0.0004 0.3084 0.0043 0.0515 0.0006 0.0160 0.0000 0.5315 0.0009 274 3 273 4 263 29

5 20 429 0.0429 0.0004 0.3101 0.0095 0.0524 0.0015 0.0169 0.0002 0.4675 0.0005 271 3 274 8 304 67

6 35 751 0.0441 0.0004 0.3141 0.0044 0.0517 0.0006 0.0168 0.0000 0.4563 0.0020 278 3 277 4 273 29

7 57 1175 0.0434 0.0004 0.3094 0.0041 0.0517 0.0006 0.0182 0.0001 0.5764 0.0019 274 3 274 4 272 27

8 93 1958 0.0440 0.0004 0.3119 0.0040 0.0514 0.0006 0.0168 0.0000 0.5005 0.0013 278 3 276 4 258 26

9 32 684 0.0439 0.0005 0.3164 0.0047 0.0523 0.0007 0.0178 0.0001 0.4435 0.0016 277 3 279 4 298 29

10 46 953 0.0439 0.0004 0.3148 0.0043 0.0520 0.0006 0.0173 0.0000 0.5473 0.0012 277 3 278 4 284 28

11 34 734 0.0436 0.0004 0.3119 0.0070 0.0519 0.0010 0.0192 0.0003 0.4173 0.0022 275 3 276 6 279 44

12 37 787 0.0441 0.0005 0.3158 0.0046 0.0519 0.0007 0.0172 0.0001 0.4669 0.0023 278 3 279 4 282 29

13 33 698 0.0439 0.0005 0.3126 0.0060 0.0516 0.0008 0.0183 0.0003 0.4248 0.0021 277 3 276 5 267 37

14 28 616 0.0439 0.0005 0.3135 0.0047 0.0518 0.0007 0.0167 0.0001 0.4013 0.0020 277 3 277 4 278 30

15 28 606 0.0446 0.0005 0.3173 0.0054 0.0516 0.0008 0.0166 0.0001 0.4441 0.0020 281 3 280 5 269 35

16 39 843 0.0442 0.0005 0.3167 0.0044 0.0519 0.0006 0.0163 0.0002 0.3852 0.0028 279 3 279 4 283 28

17 30 651 0.0443 0.0005 0.3187 0.0048 0.0521 0.0007 0.0178 0.0002 0.4172 0.0023 280 3 281 4 291 30

18 33 697 0.0446 0.0005 0.3207 0.0051 0.0522 0.0008 0.0151 0.0001 0.4839 0.0011 281 3 282 4 292 34

19 42 905 0.0442 0.0005 0.3128 0.0044 0.0514 0.0006 0.0140 0.0001 0.4860 0.0038 279 3 276 4 257 28

20 36 776 0.0443 0.0005 0.3167 0.0050 0.0518 0.0007 0.0146 0.0002 0.4479 0.0037 280 3 279 4 277 30

21 32 693 0.0449 0.0005 0.3212 0.0050 0.0519 0.0007 0.0142 0.0002 0.3977 0.0031 283 3 283 4 279 30

22 28 610 0.0442 0.0005 0.3206 0.0050 0.0526 0.0007 0.0132 0.0002 0.4562 0.0027 279 3 282 4 313 31

23 34 761 0.0438 0.0005 0.3179 0.0046 0.0527 0.0007 0.0132 0.0001 0.4129 0.0029 276 3 280 4 315 29

24 29 635 0.0441 0.0005 0.3156 0.0052 0.0519 0.0008 0.0134 0.0001 0.4435 0.0015 278 3 278 5 280 35



1 11 239 0.0420 0.0005 0.2978 0.0166 0.0515 0.0029 0.0138 0.0002 0.4826 0.0023 265 3 265 15 262 128

2 18 408 0.0412 0.0005 0.2948 0.0064 0.0519 0.0011 0.0128 0.0001 0.6818 0.0005 260 3 262 6 280 49

3 14 312 0.0418 0.0005 0.2978 0.0108 0.0516 0.0019 0.0137 0.0001 0.4468 0.0011 264 3 265 10 268 83

4 30 675 0.0415 0.0004 0.2969 0.0058 0.0519 0.0010 0.0129 0.0001 0.6395 0.0063 262 3 264 5 283 44

Page 49 of 56



Draft

5 23 532 0.0415 0.0004 0.2952 0.0052 0.0516 0.0008 0.0128 0.0001 0.4905 0.0010 262 3 263 5 268 38

6 21 464 0.0415 0.0005 0.3010 0.0051 0.0526 0.0008 0.0111 0.0001 0.6609 0.0021 262 3 267 4 312 35

7 26 588 0.0417 0.0005 0.2984 0.0052 0.0519 0.0008 0.0135 0.0001 0.4806 0.0022 263 3 265 5 283 34

8 20 459 0.0415 0.0005 0.2966 0.0076 0.0518 0.0011 0.0141 0.0002 0.5004 0.0014 262 3 264 7 278 50

9 23 527 0.0421 0.0005 0.2996 0.0062 0.0517 0.0010 0.0128 0.0001 0.4358 0.0012 266 3 266 6 270 43

10 42 935 0.0419 0.0005 0.2985 0.0046 0.0516 0.0007 0.0134 0.0001 0.5587 0.0008 265 3 265 4 268 31

11 18 415 0.0412 0.0004 0.2925 0.0053 0.0515 0.0009 0.0123 0.0001 0.6425 0.0074 260 3 260 5 265 39

12 27 599 0.0423 0.0005 0.3036 0.0050 0.0520 0.0007 0.0130 0.0001 0.6031 0.0023 267 3 269 4 288 33

13 28 642 0.0418 0.0005 0.2975 0.0047 0.0516 0.0007 0.0133 0.0001 0.4959 0.0012 264 3 264 4 269 31

14 37 745 0.0416 0.0005 0.2984 0.0046 0.0520 0.0007 0.0125 0.0000 1.0352 0.0042 263 3 265 4 286 31

15 23 514 0.0416 0.0005 0.2984 0.0050 0.0521 0.0008 0.0129 0.0001 0.6098 0.0027 263 3 265 4 289 34

16 27 592 0.0414 0.0004 0.2967 0.0047 0.0520 0.0007 0.0125 0.0000 0.7074 0.0047 262 3 264 4 284 33

17 31 706 0.0418 0.0004 0.2960 0.0044 0.0514 0.0007 0.0130 0.0000 0.5737 0.0016 264 3 263 4 258 31

18 108 1428 0.0452 0.0005 1.6798 0.0278 0.2694 0.0039 0.0197 0.0002 1.5219 0.0220 285 3 1001 17 3303 23

19 19 388 0.0426 0.0004 0.3008 0.0067 0.0512 0.0011 0.0104 0.0000 1.1140 0.0051 269 3 267 6 250 49

20 27 536 0.0425 0.0005 0.3016 0.0089 0.0515 0.0014 0.0221 0.0005 0.6176 0.0039 268 3 268 8 263 62

21 31 713 0.0414 0.0005 0.2953 0.0044 0.0517 0.0007 0.0098 0.0002 0.6149 0.0089 262 3 263 4 272 32

22 24 529 0.0419 0.0005 0.2984 0.0050 0.0516 0.0008 0.0113 0.0001 0.7657 0.0025 265 3 265 4 268 35

23 18 416 0.0417 0.0004 0.2965 0.0054 0.0516 0.0009 0.0118 0.0001 0.5575 0.0018 263 3 264 5 267 39

24 20 466 0.0418 0.0004 0.2975 0.0051 0.0516 0.0008 0.0119 0.0001 0.5079 0.0017 264 3 264 5 268 37



1 24 500 0.0413 0.0005 0.2957 0.0056 0.0519 0.0009 0.0123 0.0001 0.8938 0.0118 261 3 263 5 280 39

2 21 461 0.0414 0.0004 0.2925 0.0063 0.0512 0.0010 0.0126 0.0001 0.8040 0.0037 261 3 261 6 252 45

3 14 329 0.0413 0.0004 0.2955 0.0065 0.0519 0.0011 0.0122 0.0001 0.4746 0.0021 261 3 263 6 282 48

4 23 475 0.0413 0.0004 0.2949 0.0051 0.0518 0.0008 0.0124 0.0001 0.9015 0.0060 261 3 262 5 276 36

5 19 405 0.0414 0.0004 0.2984 0.0062 0.0523 0.0010 0.0124 0.0001 0.8530 0.0137 261 3 265 6 300 45

6 19 421 0.0415 0.0004 0.2972 0.0061 0.0519 0.0010 0.0122 0.0001 0.6998 0.0043 262 3 264 5 282 44

7 27 596 0.0412 0.0004 0.2951 0.0054 0.0520 0.0009 0.0124 0.0000 0.6589 0.0016 260 3 263 5 284 40

8 12 267 0.0413 0.0004 0.2938 0.0083 0.0516 0.0014 0.0122 0.0001 0.6957 0.0037 261 3 262 7 269 64

9 14 317 0.0417 0.0005 0.2962 0.0072 0.0516 0.0012 0.0124 0.0001 0.6513 0.0027 263 3 263 6 266 54

Page 50 of 56



Draft

10 14 309 0.0420 0.0004 0.2991 0.0073 0.0517 0.0012 0.0123 0.0001 0.6782 0.0045 265 3 266 6 272 53

11 15 322 0.0420 0.0005 0.2971 0.0087 0.0513 0.0014 0.0126 0.0001 0.6412 0.0012 265 3 264 8 255 64

12 23 524 0.0415 0.0004 0.2948 0.0052 0.0516 0.0008 0.0125 0.0001 0.5283 0.0018 262 3 262 5 267 38

13 16 346 0.0418 0.0004 0.2995 0.0108 0.0520 0.0018 0.0114 0.0001 0.7738 0.0013 264 3 266 10 286 80

14 13 303 0.0414 0.0004 0.2908 0.0065 0.0510 0.0011 0.0125 0.0001 0.5510 0.0021 261 3 259 6 239 49

15 25 556 0.0417 0.0004 0.2970 0.0050 0.0517 0.0008 0.0127 0.0001 0.6414 0.0030 263 3 264 4 273 35

16 14 315 0.0416 0.0004 0.2993 0.0070 0.0521 0.0012 0.0125 0.0001 0.4988 0.0007 263 3 266 6 291 51

17 28 555 0.0420 0.0004 0.3001 0.0050 0.0518 0.0008 0.0218 0.0001 0.6253 0.0044 265 3 267 4 278 35

18 51 842 0.0415 0.0004 0.2979 0.0046 0.0521 0.0007 0.0254 0.0001 1.0516 0.0065 262 3 265 4 289 32

19 26 477 0.0418 0.0005 0.2968 0.0053 0.0515 0.0008 0.0295 0.0003 0.6059 0.0013 264 3 264 5 264 38

20 24 447 0.0414 0.0004 0.2937 0.0056 0.0514 0.0009 0.0361 0.0002 0.4842 0.0018 262 3 261 5 259 42

21 37 665 0.0411 0.0004 0.2927 0.0064 0.0516 0.0011 0.0210 0.0001 0.9764 0.0019 260 3 261 6 268 48

22 17 299 0.0417 0.0004 0.2961 0.0087 0.0515 0.0015 0.0422 0.0003 0.4992 0.0017 263 3 263 8 265 66

23 35 620 0.0416 0.0004 0.2980 0.0054 0.0519 0.0009 0.0495 0.0002 0.4407 0.0019 263 3 265 5 282 39

24 33 585 0.0413 0.0004 0.2962 0.0047 0.0520 0.0008 0.0460 0.0003 0.4666 0.0056 261 3 263 4 287 34

Page 51 of 56



Draft

Table 2

Table 2 Major(%)and trace elements(×10-6)compositions of the monzogranites and granodiorites

Sample No. 02.19.2 02.24.1 02.39.1 02.40.2 02.25.2 02.31.1 02.32.1 02.32.2 02.33.2 02.38.1 7965.2 7907.1

Lithology monzogranite granodiorite

SiO2 73.94 71.42 71.32 72.91 69.61 69.03 67.76 67.7 68.02 68.9 66.12 66.61

Al2O3 13.11 14.42 14.44 14.28 14.78 15.09 15.32 15.86 15.78 15.48 15.93 16.01

Fe2O3 0.67 0.58 1.2 0.9 1.06 1.51 1.53 1.5 1.48 1.47 1.93 1.75

FeO 1.54 1.71 1.34 1 1.67 1.57 1.76 1.77 1.66 1.55 1.98 1.94

CaO 1.32 2.12 2.35 1.9 3.15 3.23 3.59 3.54 3.5 3.26 3.99 3.9

MgO 0.73 0.82 0.99 0.63 1.04 1.32 1.48 1.48 1.49 1.21 1.98 1.85

K2O 4.15 3.67 3.4 3.53 3.02 2.84 2.75 2.62 2.73 2.67 2.33 2.37

Na2O 3.64 4.06 3.96 4.07 4.12 4.03 4.07 4.31 4.18 4.22 4.03 4.06

TiO2 0.33 0.36 0.38 0.29 0.42 0.47 0.51 0.5 0.46 0.46 0.57 0.53

P2O5 0.081 0.088 0.098 0.076 0.12 0.12 0.13 0.12 0.12 0.13 0.14 0.14

MnO 0.056 0.059 0.061 0.052 0.072 0.063 0.067 0.067 0.064 0.069 0.072 0.07

L.O.I 0.27 0.51 0.31 0.25 0.76 0.55 0.83 0.34 0.33 0.42 0.7 0.56

Total 99.84 99.82 99.85 99.89 99.82 99.82 99.80 99.81 99.81 99.84 99.77 99.79

FeOT 2.14 2.23 2.42 1.81 2.62 2.93 3.14 3.12 2.99 2.87 3.72 3.52

Fe2O3T 2.38 2.48 2.69 2.01 2.92 3.25 3.49 3.47 3.33 3.19 4.13 3.91

Mg# 41.67 43.52 46.18 42.19 45.39 48.59 49.73 49.87 51.08 46.90 52.77 52.47

A/CNK 1.02 0.99 1.00 1.02 0.94 0.97 0.95 0.97 0.97 0.98 0.97 0.98

ALK 7.82 7.78 7.39 7.63 7.21 6.92 6.89 6.97 6.95 6.93 6.42 6.48

D.I. 88.07 83.88 82.58 86.22 79.25 77.29 75.26 75.03 75.30 77.20 70.70 71.49

Cr 4.29 4.51 5.62 4.35 4.42 7.74 9.4 8.55 9.62 7.68 17.5 19.7

Ni 3.17 3.27 4.34 3.13 4.41 6.5 7.12 7 7.92 4.76 13.8 14.4

Co 3.67 4.25 5.11 3.14 5.64 7.21 7.8 7.92 7.69 6.25 10.6 9.61

Rb 135 114 96.9 87.4 91.5 76 79.8 71.5 85.4 74.2 59.6 63.1

Cs 6.2 4.3 3.03 2.36 5.08 3.85 3.23 2.64 6.27 3.23 2.1 3.18

Sr 134 204 246 211 288 327 337 358 362 341 407 406

Ba 535 574 532 553 517 470 494 490 591 504 475 461

V 31.2 33.4 39.8 27.8 44.6 55.2 56.3 56.5 55 47.6 73.2 70

Sc 6.5 6.99 7.9 7.49 8.74 7.63 7.53 8.06 9.56 8.18 10.7 10.3

Nb 7.47 6.63 7.33 6.58 6.52 5.36 6.14 5.79 5.62 6.2 5.08 4.93

Ta 0.7 0.6 0.82 0.68 0.58 0.49 0.55 0.53 0.48 0.53 0.41 0.38

Zr 141 101 126 141 148 170 125 163 116 160 138 142

Hf 4.32 3 3.81 4.06 4.36 4.55 3.44 4.25 3.04 4.42 3.53 3.61

Ga 14.3 14.9 14.9 15 15.2 14.8 15.5 15.5 15.2 15.9 15.5 15.8

U 1.82 1.5 1.48 1.19 1.24 1.22 1.33 1.24 1.08 1.47 1.11 1.01

Th 10.5 9.28 11 7.38 8.03 6.62 6.67 6.23 5.26 8.74 5.12 5.35

La 19.6 14.4 26.5 18.1 17.4 21.7 14.4 16.6 13.7 15.5 17.8 16.3

Ce 36 26 41.2 30.8 29.6 34.6 25.2 27.8 25 27.4 29.1 27.8

Pr 4.42 3.33 5.34 3.78 4.06 4.6 3.33 3.7 3.32 3.76 3.98 3.61

Nd 15.7 12.3 18.2 12.7 15 16 12.5 13.9 12.8 14.1 15 13.7

Sm 3.11 2.49 3.4 2.41 3.04 2.8 2.57 2.74 2.72 2.81 2.9 2.66

Eu 0.45 0.58 0.64 0.52 0.66 0.72 0.71 0.77 0.77 0.74 0.85 0.82

Page 52 of 56



Draft

Gd 3.21 2.75 3.37 2.47 3.02 2.95 2.58 2.78 2.84 2.96 2.79 2.81

Tb 0.52 0.44 0.54 0.4 0.5 0.45 0.41 0.44 0.46 0.46 0.44 0.43

Dy 3.19 2.75 3.16 2.52 3 2.57 2.5 2.69 2.69 2.81 2.67 2.48

Ho 0.66 0.58 0.67 0.51 0.64 0.52 0.5 0.54 0.52 0.58 0.52 0.48

Er 1.96 1.62 1.91 1.51 1.91 1.49 1.43 1.55 1.5 1.7 1.43 1.37

Tm 0.32 0.27 0.31 0.26 0.3 0.24 0.22 0.25 0.24 0.27 0.23 0.21

Yb 2.27 2.02 2.31 1.83 2.15 1.74 1.56 1.71 1.64 1.91 1.52 1.48

Lu 0.37 0.31 0.38 0.31 0.34 0.29 0.26 0.28 0.26 0.31 0.24 0.25

Y 20 17.6 21.1 15.9 19.6 16.2 15.4 16.3 16.8 18.2 16 15.4

ΣREE 111.8 87.4 129.0 94.0 101.2 106.9 83.6 92.1 85.3 93.5 95.5 89.8

LREE/HREE 6.34 5.50 7.53 6.96 5.88 7.85 6.21 6.40 5.74 5.85 7.08 6.82

(La/Yb)N 6.19 5.11 8.23 7.09 5.81 8.95 6.62 6.96 5.99 5.82 8.40 7.90

(La/Sm)N 4.07 3.73 5.03 4.85 3.70 5.00 3.62 3.91 3.25 3.56 3.96 3.96

(Gd/Lu)N 1.07 1.10 1.10 0.98 1.10 1.26 1.23 1.23 1.35 1.18 1.44 1.39

δEu 0.44 0.68 0.58 0.65 0.67 0.77 0.84 0.85 0.85 0.79 0.92 0.92

Page 53 of 56



Draft

Table 3

Table 3 Sm-Nd and Rb-Sr isotopic compositions of the monzogranites and granodiorites

Sample Age (Ga) Rb Sr 87Sr/86Sr (87Sr/86Sr)i Sm Nd 143Nd/144Nd (143Nd/144Nd)i TDM(Ga) T2 DM(Ga) εNd fSm/Nd f(%)

02.19.2 0.27 135 134 0.710659 0.699458 3.11 15.7 0.512758 0.512536601 0.678807 0.648 4.81 -0.36 0.937

02.24.1 0.27 114 204 0.71135 0.705137 2.49 12.3 0.512748 0.51252174 0.718361 0.671 4.52 -0.35 0.931

02.39.1 0.27 96.9 246 0.711324 0.706944 3.4 18.2 0.512743 0.512534204 0.65213 0.652 4.76 -0.40 0.936monzogranite

02.40.2 0.27 87.4 211 0.711654 0.707048 2.41 12.7 0.512742 0.512529906 0.66673 0.658 4.68 -0.39 0.934

02.31.1 0.26 76 288 0.704934 0.702111 2.8 15 0.512775 0.512574102 0.600501 0.600 5.29 -0.40 0.946

02.32.1 0.26 79.8 327 0.705054 0.702443 2.57 16 0.512768 0.512595129 0.52189 0.567 5.70 -0.48 0.953

02.32.2 0.26 71.5 337 0.705594 0.703324 2.74 12.5 0.512763 0.512527088 0.789213 0.675 4.37 -0.30 0.928granodiorite

02.33.2 0.26 85.4 358 0.705537 0.702985 2.72 13.9 0.512758 0.512547397 0.667338 0.643 4.77 -0.37 0.936Note: f(%) is the proportion of mantle-derived components in the crust-mantle binary mixtures calculated by DePaolo et al. (1991) method. f=(Ndc/Ndm)/[(Ndc/Ndm)+( εm-εs)/ ( εs-εc), Ndc and Ndm represent abundance of Nd in crustal and mantle endmember respectively. εs, εc and εm represent εNd(t) values of sample, crust and mantle, Ndc=43.4×10-6, Ndm=15×10-6, εc=-14.24, εm=8.54.

Page 54 of 56



Draft

Table 4

Table 4 Zircon Hf isotopic data of the monzogranite (02TW19) and granodiorite (01TW32)

02TW19 Age (Ma) 176Yb/177Hf 176Lu/177Hf 176Hf/177Hf 176Hf/177Hfi εHf(0) εHf(t) TDM (Ma) TC DM (Ma)

1 271 0.0587 0.0017 0.282963 0.282954 6.7 12.4 417 5022 276 0.0820 0.0023 0.282996 0.282984 7.9 13.6 376 4303 270 0.0561 0.0016 0.282957 0.282949 6.5 12.2 425 5154 271 0.0797 0.0022 0.282935 0.282925 5.8 11.4 463 5695 270 0.0837 0.0024 0.282997 0.282985 8.0 13.5 374 4316 269 0.0729 0.0021 0.282982 0.282972 7.4 13.0 393 4637 271 0.1456 0.0040 0.282855 0.282835 2.9 8.2 610 7728 275 0.0612 0.0018 0.282968 0.282959 6.9 12.7 411 4889 270 0.0847 0.0026 0.282910 0.282897 4.9 10.4 506 63310 267 0.0988 0.0029 0.283110 0.283095 11.9 17.3 211 18211 269 0.0613 0.0017 0.282903 0.282894 4.6 10.2 504 63912 269 0.0637 0.0018 0.282968 0.282959 6.9 12.5 412 49313 271 0.0460 0.0014 0.282986 0.282979 7.6 13.3 381 44514 269 0.0577 0.0016 0.282990 0.282982 7.7 13.4 376 43915 266 0.0535 0.0015 0.282947 0.28294 6.2 11.8 437 53716 271 0.0495 0.0013 0.283008 0.283002 8.4 14.1 348 394

02TW32 Age (Ma) 176Yb/177Hf 176Lu/177Hf 176Hf/177Hf 176Hf/177Hfi εHf(0) εHf(t) TDM (Ma) TC DM (Ma)

1 261 0.0715 0.0020 0.282704 0.282694 -2.4 3.0 797 1097 2 261 0.0740 0.0021 0.282858 0.282848 3.0 8.4 576 751 3 260 0.0589 0.0017 0.282898 0.282890 4.5 9.9 510 654 4 261 0.0614 0.0018 0.282905 0.282896 4.7 10.1 503 641 5 265 0.0562 0.0017 0.282838 0.282830 2.3 7.9 597 788 6 262 0.0466 0.0013 0.282907 0.282900 4.8 10.3 493 630 7 264 0.1420 0.0031 0.282921 0.282905 5.3 10.5 498 618 8 261 0.0284 0.0008 0.282928 0.282924 5.5 11.1 456 576 9 263 0.0926 0.0023 0.282896 0.282884 4.4 9.8 524 666 10 263 0.0599 0.0015 0.282958 0.282950 6.6 12.1 423 516 11 265 0.0770 0.0021 0.282898 0.282887 4.5 9.9 517 657 12 262 0.0724 0.0018 0.282901 0.282892 4.6 10.0 509 649 13 264 0.0801 0.0019 0.282896 0.282886 4.4 9.8 517 661 14 263 0.0616 0.0015 0.282981 0.282973 7.4 12.9 389 463 15 263 0.0707 0.0017 0.283004 0.282995 8.2 13.7 358 413 16 261 0.0846 0.0019 0.282916 0.282907 5.1 10.5 487 615

Table 5

Table 5 Result from saturated Zr thermometer of the monzogranites and granodioritessample Zr(10-6) M Tzr(0C)

02.19.2 141 1.4 779 02.24.1 101 1.5 745 02.39.1 126 1.5 764 monzogranite

02.40.2 141 1.4 778 02.25.2 148 1.6 768 02.31.1 170 1.6 782 02.32.1 125 1.7 752 02.32.2 163 1.6 776 02.33.2 116 1.6 749 02.38.1 160 1.6 778 7965.2 138 1.7 760

granodiorite

7907.1 142 1.6 764

Note: TZr = 129000 /［2.95 + 0.85M + ln( 469000 /Zrsamle) ］，M is some cationic ratios in rock, M = ( Na + K + 2Ca) /( Al × Si).

Page 55 of 56



DraftLith

ospher

ic m

antle

Lithospheric mantle

breakoff slab

Baiheshan accretio

nary complex

Baishan arc

Continen

tal c

rust

junenile crustal MASH zone

Carboniferousgranitoids Permian granitoids

Upwelling asthenosphere

Continental crust

CarboniferousBaishan Formation

Permian Shuangbaotang Formation

unconformity

N S

W

E

Permian (277-262Ma)

Extension

Oceanic crust Asth

enosp

here m

antle

Asthenosphere mantle

Schematic diagram showing the petrogenetic model for the Permian granitoids in northern Beishan orogen

Page 56 of 56



draft · 2020-03-24 · draft 21 granitoids were derived from common sources of melting from the...

Documents