Early Jurassic Monzogranite-Tonalite Association from the Southern Zhangguangcai Range: Implications for Paleo–Pacific Plate Subduction Along Northeastern China

Home , Monzogranite

Early Jurassic monzogranite-tonalite association from the southern Zhangguangcai Range: Implications for paleo–Pacific plate subduction along northeastern China

Jiang-Feng Qin1,*, Shao-Cong Lai1, Yong-Fei Li2, Yin-Juan Ju1, Ren-Zhi Zhu1, and Shao-Wei Zhao1 1STATE KEY LABORATORY OF CONTINENTAL DYNAMICS, DEPARTMENT OF GEOLOGY, NORTHWEST UNIVERSITY, XI’AN 710069, CHINA 2SHENYANG INSTITUTE OF GEOLOGY AND MINERAL RESOURCES, SHENYANG 110032, CHINA

ABSTRACT

The initiation time and tectonic responses of paleo–Pacific plate subduction beneath the Eurasian continent remain controversial. In this paper we report on Early Jurassic (201–198 Ma) monzogranite-tonalite association from the southern Zhangguangcai Range, northeastern China. Zircon laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) U-Pb dating indicates that the monzogranite and tonalite have identical 206Pb/208U ages of 201 ± 2 (mean square of weighted deviates, MSWD = 1.2, 2s) and 198 ± 3 Ma (MSWD = 3.2, 2s), respectively. The monzogranite and tonalite display different geochemical features, suggesting that they were derived from two distinct

source regions. The monzogranite displays high SiO2, K2O, and Rb contents, as well as depleted whole-rock Sr-Nd-Pb isotopic compositions,

i.e., eNd(t) = +8.3 to +11.7, with single-stage Nd model ages of 0.30–0.05 Ga. Zircons from the monzogranite also have depleted Lu-Hf isotopic compositions, and these contradictory geochemical features suggest that the monzogranite may be derived from melting of mid-oceanic

ridge basalt (MORB)–sediment mélanges in subduction zone. The Na-rich tonalite has lower SiO2 and higher TiO2 contents. In combination with their relatively evolved Sr-Nd-Pb isotopic compositions and zircon Lu-Hf isotopic compositions, it can be considered that the tonalite was derived from juvenile basaltic crust in an active continental margin. Considering other Triassic to Jurassic mafic intrusive rocks and I-type granites in the Zhangguangcai Range, we propose that the Early Jurassic monzogranite-tonalite association in the Shihe area was caused by the westward subduction of the paleo–Pacific plate beneath northeastern China.

LITHOSPHERE; v. 8; no. 4; p. 396–411; GSA Data Repository Item 2016171 | Published online 21 June 2016 doi:10.1130/L505.1

INTRODUCTION Lesser Xing’an–Zhangguangcai Range were mostly formed during the Jurassic (190–150 Ma), with a small amount in the Paleozoic, and the The Lesser Xing’an–Zhangguangcai Range is located in the eastern Jurassic granitic rocks are considered to have been caused by subduc- part of the Central Asian Orogenic Belt (CAOB) (Fig. 1A). The CAOB tion of the paleo–Pacific plate beneath the Eurasian continent (Wu et is considered to result from collision between the North China block and al., 2011). The following two geological problems in this region are still Siberia block during the Late Permian (Li, 2006) or Early Triassic (Xu debated. (1) Initiation time of the subduction of the paleo–Pacific plate. et al., 2009). Unlike other parts of the CAOB, northeastern China was Based on zircon U-Pb dating of the high-pressure metamorphic mafic significantly affected by the subduction of the paleo–Pacific plate in the rocks, Zhou et al. (2009) argued that the Heilongjiang Complex records Jurassic (Xu et al., 2009; Wu et al., 2011). Phanerozoic granitic rocks in the time when northward movement of the combined Mongolia–North northeastern China are exposed over an area of ~200,000 km2, and they China block toward Siberia was waning, and was surpassed by the onset display depleted Sr-Nd isotopic compositions, which indicate significant of Pacific accretion from the east. (2) The transformation mechanism Phanerozoic crust growth (Han et al., 1997; Jahn et al., 2000; Jahn, 2010; from the paleo-Asian tectonic regime to the paleo-Pacific regime. Xu et Wu et al., 2000, 2002, 2003, 2011; Guo et al., 2010). However, the crustal al. (2009) reported Early Jurassic volcanic rocks from the eastern part growth model and petrogenesis of these granitic rocks remain controversial. of the Jilin-Heilongjiang area, and detailed geochemistry indicates that The granitic rocks with depleted Sr-Nd isotopic compositions were consid- these volcanic rocks were derived from juvenile crust in an extensional ered to be formed by fractional crystallization of mantle-derived melt (Han setting. It is intriguing as to whether the early Mesozoic granitic rocks et al., 1997), mixing of crust-derived and mantle-derived melts (Jahn et al., and related volcanic rocks in the Zhangguangcai Range were caused by 2000), or remelting of preexisting juvenile basaltic rocks (Wu et al., 2002). subduction of the paleo–Pacific oceanic slab. The Lesser Xing’an–Zhangguangcai Range is considered to result In this paper we report zircon U-Pb ages, geochemistry, Sr-Nd-Pb isoto- from collision between the Songneng block and Jiamusi block in the pic compositions, and zircon Lu-Hf isotopic composition of an Early Juras- Paleozoic or early Mesozoic (Zhou et al., 2009; Xu et al., 2009; Wu sic tonalite-monzogranite suite from the Shihe area, in the southern part of et al., 2011; Zhou and Wilde, 2013; Shao et al., 2013). Detailed geo- the Zhangguangcai Range. Detailed geochemical investigations indicate chronology works (Wu et al., 2011) indicate that the granitoids in the that the Na-rich tonalite was derived from juvenile basaltic crust, while the monzogranite was formed by partial melting of sediment–mid-oce- *[email protected] anic ridge basalt (MORB) mélanges in the subduction accretion complex.

Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/8/4/396/3040314/396.pdf by guest on 27 September 2021 Early Jurassic monzogranite-tonalite from northeastern China | RESEARCH

A 80N60N 40N 180E PO 160E F8 40E Russia Russia 80E 120E Le s s F6 e r X in g ’a n Siberian Ra K

AB i East-European n a g Mongolia e e m O CP Qiqihar Paleo-Asian 30N u e sz Orogens MO Rang g P PO n e aleo-Asian a P Bl Fig.1B g’an n Fig.2 in F5 R o Basi ai c t X k PPO iao Harbin c F1 Orogenic belt ngl ng Grea So Mudanjiang Sino-Korean 20N F7 PO ggua F3 n Changchun PTO/TO ha F2 PTO/TO Z F4 Arabian 10N Shenyang Indian PPO PO

North China Block Jinzhou 10N

60E 140E rea N 120E Ko Beijing Present subduction 80E B 100E 1200km Precambrain continents Phanerozoic orogens PO-modern pacific Paleo-Asian sutures Paleo-Pacific sutures PPO-Paleo-Pacific PTO-Paleo-Tethys MMO-Mongolian-Okhotsk Orogenic belt 0 200km Paleo-Tethys sutures Tethys sutures TO-Tethys CPAB-Circum Pacific Accretionary belt

Figure 1. (A) Geological map of Eurasia continent. (B) Geological map of northeastern China (revised from Wu et al., 2011). F1—Mudanjiang fault; F2—Dunhua-Mishan fault; F3—Yitong-Yilan fault; F4—Chifeng-Kaiyuan fault; F5—Hegenshan-Heihe fault; F6—Tanyuan-Xiguitu fault; F7—Xar Moron- Changchun suture zone; F8—Mongol-Okhotsk fault.

These results can promote our understanding of the early Mesozoic sub- The Shihe pluton is located in the eastern part of the Shangzhi area duction process of the paleo–Pacific oceanic slab along northeastern China. in the southern Zhangguangcai Range (Fig. 2), which was considered to result from collision between the Songneng and Kiamusze block (Zhou GEOLOGICAL BACKGROUND AND FIELD GEOLOGY et al., 2009; Zhou and Wilde, 2013; Shao et al., 2013). The granites and associated volcanic rocks intruded into the Permian Tangjiatun formation, Northeastern China is located in the eastern part of the CAOB (Şengör et which consists of deformed intermediate-felsic volcanic rocks. Accord- al., 1993; Jahn et al., 2000; Wu et al., 2011), where previous work revealed ing to field observations, monzogranite and tonalite were in the Shihe two stages of evolution under different tectonic regimes (Wu et al., 2002, pluton, while the mafic enclaves were mainly hosted in the tonalities 2011; Li, 2006; Xu et al., 2009). Northeastern China consists of the Erguna (Fig. 3). The sampling locations are shown in Figure 2; the monzogran- terrane in the northwest, the Xing’an and Songliao terranes in the center, ite samples were collected from the western Shihe village (44°52′22″N, and the Liaoyuan terrane in the southeast (Fig. 1B). The Lesser Xing’an– 128°40′26″E), while the tonalite samples were collected from the eastern Zhangguangcai Range is located at the boundary between the Songliao Shihe Village (44°51′43″N, 128°42′30″E). The monzogranite display and Jiamusi terranes. The Songliao terrane is overlain by the Mesozoic medium- to coarse-grained textures, and mainly consist of alkali feldspar Songliao basin, and most of the basement beneath the Songliao basin is (35–40 vol%), plagioclase (25–35 vol%), biotite (10–15 vol%), quartz composed of Paleozoic–Mesozoic granitoids and Paleozoic strata (Wu et (25–30 vol%), and accessory minerals including zircon, apatite, and mag- al., 2000, 2011; Xu et al., 2013) with minor Proterozoic granitoids (Pei et netite. The plagioclase is 1.0–3.0 mm long and exhibits well-developed al., 2011). The Jiamusi massif consists of the Mashan and Heilongjiang twinning and concentric zoning (Fig. 3C). Biotite is the predominant complexes, and the deformed granitoids in the Mashan complex have a mafic mineral in the monzogranite; most of the biotites were corroded peak metamorphic age of ca. 500 Ma (Wilde et al., 2000). Detailed zircon and display subeuhedral shapes (Fig. 3C). The tonalite samples from the U-Pb dating of the blueschist facies metamorphosed pillow basalts (Zhou Shihe area are medium grained, and consist of plagioclase (35–45 vol%), et al., 2009) indicates that these basaltic rocks are Late Triassic, and are alkali feldspar (15–20 vol%), quartz (5–15 vol%), amphibole (10–15 considered to be a mélange along the suture between the Jiamusi massif and vol%), and accessory minerals including zircon, apatite, and magnetite Songliao terrane (Wu et al., 2011; Zhou et al., 2009; Zhou and Wilde, 2013). (Fig. 3D). Plagioclase in the tonalite has oligoclase composition; they Voluminous granites and some Proterozoic to Paleozoic metamor- display the albite twin law, and amphibole fragments were included in phic rocks occur in the Zhangguangcai Range. Proterozoic strata in the the large oligoclase crystals. Mafic enclaves hosted in the tonalite range Zhuangguangcai Range include the Dongfenshan and Xingdong groups. from 10 to 60 cm (Fig. 3B), are round, and have transitional contacts Paleozoic strata include the Early Devonian Heilonggong Formation. with the host tonalite. They display hypidiomorphic texture, with large Mesozoic strata consist of the Triassic Fengshantun Formation, the Middle amount of biotite clusters and magnetite (Figs. 3E, 3F); considering Jurassic Taiantun Formation, the Late Jurassic Maoershan Formation, and these petrographic features, we argue that these mafic enclaves may the Early Cretaceous Banfangzi, Guanghua, Ningyuancun, and Taoqihe represent a mafic mineral cumulate during the crystallization process of Formations (Zhou and Wilde, 2013). the tonalitic magma.

LITHOSPHERE | Volume 8 | Number 4 | www.gsapubs.org 397

Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/8/4/396/3040314/396.pdf by guest on 27 September 2021 JIANG-FENG QIN ET AL.

128° 35′ 128° 40′ 128° 45′ 128° 50′ 128°55′

Kaidaotun Yabuli Yuchizi Hufeng

44° 55′ 44°55′

Shihe

Balitun 44° 50′ 44°50′

Lengshan 128° 35′ 128° 40′ 128° 45′ 128° 50′ 128° 55′ N Jurassic volcanic coarse-grained tonalite granodiorite sampling locations 0123km rocks monzogranite Proterozoic quartz veins Faults rail way rocks

Figure 2. Geological map of the Early Jurassic Shihe pluton from the southern Zhangguangcai Range.

ANALYTICAL METHODS The zircon grains were separated using conventional heavy liquid and magnetic techniques. Representative zircon grains were hand-picked and All of the analyses for this paper were performed at the State Key mounted on epoxy resin discs, then polished and coated with carbon. Inter- Laboratory of Continental Dynamics, Northwest University, China. For nal morphology was examined using cathodoluminescent (CL) prior to major and trace element analysis, fresh chips of whole-rock samples were U-Pb and Lu-Hf isotopic analyses. Laser ablation (LA) ICP-MS zircon powdered to 200 mesh using a tungsten carbide ball mill. Major and trace U-Pb analyses were conducted on an Agilent 7500a ICP-MS equipped with elements were analyzed using X-ray fluorescence (Rikagu RIX 2100) a 193 nm laser, following the method of Yuan et al. (2004). The 207Pb/206Pb and inductively coupled plasma–mass spectrometry (ICP-MS) (Agilent and 206Pb/238U ratios were calculated using the GLITTER data reduction 7500a), respectively. Analyses of U.S. Geological Survey and Chinese software program (http://www.glitter-gemoc.com/), which was corrected national rock standards (BCR-2, GSR-1, and GSR-3) indicate that both using Harvard zircon 91500 as external calibration. These correction fac- the analytical precision and accuracy for major elements are generally tors were then applied to each sample to correct for both instrumental mass better than 5%. For trace element analysis, sample powders were digested bias and depth-dependent elemental and isotopic fractionation. The detailed

using an HF + HNO3 mixture in high-pressure Teflon bombs at 190 °C analytical technique was described in Yuan et al. (2004). Common Pb con- for 48 h. The analytical precision was better than 10% for most of the tents were evaluated using the method described by Andersen (2002). The trace elements. age calculations and plotting of concordia diagrams were performed using Whole-rock Sr-Nd-Pb isotopic data were obtained using a Nu Plasma ISOPLOT (version 3.0; Ludwig, 2003). The errors quoted in the tables HR multicollector (MC) mass spectrometer. The Sr and Nd isotopic frac- and figures are at the s2 levels. In situ zircon Hf isotopic analyses were tionation was corrected to 87Sr/86Sr = 0.1194 and 146Nd/144Nd = 0.7219, conducted using a Neptune MC-ICP-MS equipped with a 193 nm laser. respectively. During the analysis period, the NIST SRM 987 standard During analyses, a laser repetition rate of 10 Hz at 100 mJ was used and yielded an average value of 87Sr/86Sr = 0.710250 ± 12 (2s, n = 15), and spot sizes were 44 mm. The 176Yb/172Yb value of 0.5887 and mean Yb value the La Jolla standard gave an average of 143Nd/144Nd = 0.511859 ± 6 obtained during Hf analysis on the same spot were applied for the interfer- (2s, n = 20). Whole-rock Pb was separated by an anion exchange in ence correction of 176Yb on 176Hf (Iizuka and Hirata, 2005). The detailed HCl-Br columns, and the Pb isotopic fractionation was corrected to analytical technique was described by Yuan et al. (2008). During analyses, 205Tl/203Tl = 2.3875. Within the analytical period, 30 measurements of the 176Hf/177Hf and 176Lu/177Hf ratios of the standard zircon (91500) were NBS 981 gave average values of 206Pb/204Pb = 16.937 ± 1(2s), 207Pb/204Pb 0.282294 ± 15 (2s, n = 20) and 0.00031, similar to the commonly accepted = 15.491 ± 1 (2s), and 208Pb/204Pb = 36.696 ± 1 (2s). The BCR-2 stan- 176Hf/177Hf ratio of 0.282302 ± 8 and 0.282306 ± 8 (2s) measured using the 206 204 207 204 dard gave Pb/ Pb = 18.742 ± 1 (2s), Pb/ Pb = 15.620 ± 1 (2s), solution method. The notations of eHf(t) value, fLu/Hf (f—different constant 208 204 and Pb/ Pb = 38.705 ± 1 (2s). Total procedural Pb blanks were in of Lu and Hf), single-stage model age (TDM1—depleted mantle), and two-

the range of 0.1–0.3 ng. stage model age (TDM2) are as defined in Yuan et al. (2008).

398 www.gsapubs.org | Volume 8 | Number 4 | LITHOSPHERE

mafic enclaves

f CDp e l la d quartz g s i o p c la a se r K-feldspar se uartz cla q gio pla te ti o e i ol b ib ph am

0.5 mm 0.5 mm EF p la g quartz io c la biotite se biotite biotite ar magnetite sp ld fe K- magnetite biotite

0.5 mm 0.5 mm

Figure 3. Field photographs and microscope images of samples from Shihe pluton. (A) Monzogranite. Diameter of coin is 1 cm. (B) Tonalite. (C) Micro- scope image of monzogranite. (D) Microscope image of tonalite. (E, F) Microscope images of mafic enclaves hosted in the tonalite.

LITHOSPHERE | Volume 8 | Number 4 | www.gsapubs.org 399

Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/8/4/396/3040314/396.pdf by guest on 27 September 2021 JIANG-FENG QIN ET AL.

RESULTS 3:1–5:1. Most of the grains display well-developed oscillatory zoning (Fig. 4A). Of 36 spots, 7 (4, 8, 12, 16, 21, 28, and 29) display disconcor- Zircon LA-ICP-MS U-Pb Dating dant U-Pb ages. Other 29 spots have Th = 117–1144 ppm and U = 163– 1507 ppm, with Th/U ratios of 0.29–1.45. These grains have 206Pb/238U Zircons from the monzogranite (STH-1), tonalite (STH-2), and mafic ages of 184 ± 6 Ma to 212 ± 6 Ma (Fig. 4D), yielding a weighted mean enclaves (STH-2E) that were hosted in the tonalite from the Shihe pluton age of 201 ± 2 Ma (mean square of weighted deviates, MSWD = 1.2, were selected for LA-ICP-MS U-Pb dating and Lu-Hf isotopic analysis. 2s), which represents the crystallization age of the monzogranite in the Zircon cathodoluminescence (CL) images and U-Pb isotopic composi- Shihe area. tions of the zircon from the Shihe tonalite and monzogranite are presented Zircons from the tonalite (STH-2) are subhedral to euhedral, light in Figure 4, and the U-Th-Pb isotope data are listed in Table DR1 in the yellowish-brown to colorless, with crystal lengths of 100–150 mm and GSA Data Repository1. aspect ratios of 1:1–2:1. Most of the grains are gray and display well- Zircons from monzogranite (STH-1) are euhedral, light yellow- developed oscillatory zoning in CL images (Fig. 4B). Of 36 spots, 11 ish-brown to colorless, long prismatic crystals, with aspect ratios of display disconcordant U-Pb ages. The other 25 spots have U contents of 273–1404 ppm and Th contents of 172–1173 ppm, with Th/U ratios of 0.28–1.20. They also have concordant 206Pb/238U ages of 188 ± 3 Ma to 1 GSA Data Repository Item 2016171, Zircon U-Pb isotopic results of Shihe pluton, is available at www.geosociety.org/pubs /ft2016.htm, or on request from editing@ 213 ± 6 Ma, yielding a weighted mean age of 198 ± 3 Ma (MSWD = 3.2, geosociety.org. 2s), representing the crystallization age of the tonalite in the Shihe area.

(A) STH-1

202± 3Ma 203± 3Ma 199± 6Ma 207± 6Ma 199±6Ma 193± 6Ma +11.7 203± 6Ma +12.8 +11.7 +9.5 +9.8 +14.0 +11.3

198± 6Ma 219± 15Ma 206±6Ma 158± 6Ma 196± 6Ma 195± 9Ma +9.2 +16.2 192± 6Ma +8.0 +12.9 +15.0 +10.1 +11.8

(B) STH-2 207± 3Ma 203± 3Ma 194±3Ma 178± 3Ma

+13. 8 +15. 3 +9.4 +13. 8

200± 3Ma 222± 6Ma 193± 3Ma 200± 3Ma 207± 3Ma +16. 4 +10. 6 +15. 8 +12. 9 +9.2 203± 3Ma +13. 2 +14. 5 226± 3Ma

204±6Ma 195±3Ma 196± 6Ma 189± 6Ma

197± 6Ma 204± 3Ma 205± 6Ma 202±6Ma

100 μm

Figure 4. (A– C) Cathodoluminescence (CL) images of representative zircons. (Continued on following page.)

400 www.gsapubs.org | Volume 8 | Number 4 | LITHOSPHERE

206 238 0.038 (D) STH-1(240 G) STH-1 260 Pb/U weighted mean age is 201± 2Ma (n=29, MSWD=1.2)

0.036 240 220

U 0.034 8 3 /

b 220 P

62 0.032 200 20

200 0.030

180 0.028 180

0.026 0.05 0.15 0.25 0.35 160 2072Pb/U35

(E) STH-2 230 (H) STH-2 0.035 2062Pb/U38 weighted mean age is 198± 3Ma (n=25, MSWD=3.3) 220

U 210

8 0.033 3 210 b/ P 62 20 0.031 200

190 190 0.029

180

0.027 0.16 0.18 0.20 0.22 0.24 0.26 0.28 0.30 170 2072Pb/U35

(F) STH-2E (I) STH-2E 206238 250 Pb/U weighted mean age is 0.034 196± 3Ma (n=22, MSWD=1.11) 210

0.032 230 38 /U

Pb 0.030 190 210 20 62

0.028 190

170

0.026 0.12 0.16 0.20 0.24 0.28 0.32 0.36 170 2072Pb/U35 Figure 4 (continued). (D–I) Laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) U-Pb zircon concordia diagrams for the monzogranite (STH-1), tonalite (STH-2), and mafic enclaves (STH-2E) from the Shihe pluton. Circles indicate the locations of LA–multicollec-

tor–ICP–MS Hf analyses; numbers in circles refer to eHf(t) values (see text). All eHf(t) values of enclave and host diorites were calculated according their crystallization age. MSWD—mean square of weighted deviates.

LITHOSPHERE | Volume 8 | Number 4 | www.gsapubs.org 401

Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/8/4/396/3040314/396.pdf by guest on 27 September 2021 JIANG-FENG QIN ET AL.

Zircons (STH-2E) from the mafic enclaves hosted in the tonalite dis- Sr-Nd-Pb Isotopic Compositions play subeuhedral to euhedral, light yellowish-brown to colorless crystals; as shown in the CL images, most grains display oscillatory zoning (Fig. Whole-rock Sr-Nd-Pb isotopic compositions are given in Tables 2 4C). Of 36 spots, 14 (1, 2, 8, 12, 13, 16, 17, 18, 22, 29, 30, 32, 33, and and 3. Initial isotopic values were calculated according to the LA-ICP- 35) display disconcordant U-Pb ages. The other 22 spots display concor- MS zircon U-Pb dates for the monzogranite and tonalite. Whole-rock Nd dant U-Pb ages, have Th = 133–3031 ppm, U = 180–1880 ppm, and high model ages were calculated using the model of DePaolo (1981). Th/U ratios of 0.51–1.13, suggesting a magmatic origin. These 22 spots The monzogranite (STH-3, STH-4) samples display higher Rb (89.7– 206 238 87 86 have Pb/ U ages of 186 ± 3 Ma to 230 ± 6 Ma (Fig. 4F), yielding a 100 ppm) and lower Sr (176–203 ppm) contents; they have ( Sr/ Sr)i = 143 144 weighted mean age of 198 ± 3 Ma (MSWD = 1.1, 2s). The geological 0.704118–0.704207, high Nd/ Nd ratios of 0.512905–0.512929, eNd(t) significance of this age should be carefully considered; according to the values of +8.3 to +11.7, and single-stage Nd model ages of 0.05–0.30 Ga field and microscope photo of the mafic enclaves (biotites clusters in the (Table 2). The tonalite samples (STH-2-3, STH-2-5) have high Sr contents 87 86 143 144 mafic enclaves), we argued that the zircons in the mafic enclaves were (580–583 ppm), with ( Sr/ Sr)i = 0.704625–0.704631, Nd/ Nd ratios

from the host tonalite. of 0.512572–0.512878, eNd(t) values of +1.9 to +3.3, and two-stage Nd model ages of 0.65–0.75 Ga. 87 86 Major and Trace Element Chemistry As shown in the eNd(t) versus ( Sr/ Sr)i diagram (Fig. 7A), the monzogranite and tonalite samples display Sr-Nd isotopic compositions simi- Major and trace element analyses of monzogranite and tonalite from lar to mid-oceanic ridge basalt (MORB) (Tribuzio et al., 2004; Xu and the Shihe pluton are listed in Table 1. Castillo, 2004), adakite rocks from Cenozoic subduction zones (Defant, 1990; Sajona et al., 2000), and adakite derived from partial melting Monzogranite of newly underplated basaltic crust (Petford and Atherton, 1996) and clearly differ from the Triassic igneous rocks in the northern margin of

Three monzogranite samples display high SiO2 (73.21–74.68 wt.%) the North China craton (Yang et al., 2007, 2012), suggesting a juvenile

contents, and low TiO2 (0.19–0.21 wt.%) and Al2O3 (13.90–14.40 wt.%) source region. contents, low A/CNK values (1.03 to 1.04). The monzogranite samples are In the 206Pb/204Pb–207Pb/204Pb and 206Pb/204Pb–207Pb/204Pb diagrams

sodic, with Na2O = 4.30–4.53 wt.%, K2O = 3.57–3.83 wt.%, and Na2O/ (Figs. 7B, 7C), the monzogranite and tonalite plot in the transitional zone

K2O = 1.12–1.27, all the samples plot in the calc-alkaline field. As shown between lower continental crust and MORB, also indicating a juvenile 206 204 in the trace element ratios versus SiO2 or SrN diagrams, the monzogranite source region. The monzogranite samples have ( Pb/ Pb)i = 18.463– samples display a significant compositional gap with the tonalite (Fig. 5). 18.525, (207Pb/204Pb)i = 15.558–15.562, and (208Pb/204Pb) = 37.924–37.928. In the chondrite-normalized rare earth element (REE) patterns (Fig. 6A), The tonalite samples have (206Pb/204Pb)i = 18.401–18.641, (207Pb/204Pb)i = the monzogranite samples show slight enrichment in light REEs, with 15.555–15.561, and (208Pb/204Pb) = 37.945–37.958 (Table 3).

low (La/Yb)N ratios of 6.6–11.4, and negative Eu anomalies of 0.66–0.75; in addition, they have low total REE contents (SREE) of 91.22–122 ppm. Zircon Chemistry and Lu-Hf Isotopic Composition Furthermore, the monzogranite samples display flat heavy REE patterns,

(Dy/Yb)N = 0.84–0.99. In primitive mantle–normalized element diagrams Zircons from the tonalite and monzogranite dated by U-Pb were also (Fig. 6C), the monzogranite samples show troughs in Nb, Ta, Sr, P, and Ti, analyzed for Lu-Hf isotopes of the same domain, and the results are listed 176 177 and spikes in Rb, Ba, Th, and K, with K/Rb = 296–355, Ba/Th = 81–97, in Table 4. Initial Hf/ Hf ratios and eHf(t) values of the magmatic Juras- Rb/Sr = 0.45–0.51, and Nb/Ta = 8.27–12.23, similar to granites derived sic zircons were calculated according to their 206Pb/238U ages. Figure 8A

from continental crust (Pitcher, 1997). shows eHf(t) values versus crystallization ages of the monzogranite and tonalite in the Shihe pluton. Tonalite We selected 30 zircon grains from the monzogranite (STH-1) for Lu-Hf isotope analysis. Of 30 spots, 7 (4, 8, 12, 16, 21, 28, and 29) display dis-

Eight tonalite samples from the Shihe pluton have relatively low SiO2 concordant U-Pb ages, and their Lu-Hf isotopic compositions have no

(63.78–67.39 wt%) contents, high TiO2 (0.35–0.44 wt%), Al2O3 (17.18– geological significance. The other 23 grains display depleted Hf isotopic

19.48 wt%), and high A/CNK values of 1.02–1.04. The samples have Na2O compositions with eHf(t) values ranging from +7.8 to +18.2, with corre-

= 5.92–6.72 wt%, K2O = 1.66–2.22 wt%, and Na2O/K2O = 2.90–3.54. sponding single-stage Hf model ages of 120–542 Ma. The #26 spot has

They have MgO contents of 0.69–0.83 wt% and Fe2O3total = 2.32–2.75 the highest eHf(t) values (+18.2) with a single-stage Hf model age of 120 wt% with Mg# ranging from 36.7 to 40.1. In the chondrite-normalized Ma, which is significantly younger than the zircon U-Pb age. Furthermore, REE diagram, the tonalite samples display enrichment in light REE (Fig. this spot has a higher 176Yb/177Hf ratio of 0.00028; therefore, the data

6C), with (La/Yb)N ratios of 7.4–10.5. Most of the samples (except STH- should be used with caution. 2-1) display positive Eu anomalies (Eu/Eu* = 1.05–1.40). The tonalite Zircons from the tonalite (STH-2) also display depleted Lu-Hf isotopic

also have flat heavy REE patterns with low (Dy/Yb)N ratios of 0.62–1.07; compositions (Table 4). Of 30 spots, 9 display disconcordant U-Pb ages their SREE contents (117–216 ppm) are slightly higher than those of the (Table DR1), and the other 21 grains display depleted Hf isotopic com-

monzogranite samples. As shown in the primitive mantle–normalized positions, with eHf(t) values of +9.4 to +17.8 and single-stage Hf model

spider diagrams (Fig. 6D), the tonalite samples are enriched in Rb, Ba, ages ranging from 463 to 133 Ma. Spots #1, #2, and #16 have higher eHf(t) and Th, and depleted in Nb, Ta, Sr, and Ti, displaying the typical geo- values and younger single-stage Hf model ages of 160–133 Ma, signifi- chemical features of crustal-derived rocks or island-arc volcanic rocks cantly younger than their zircon U-Pb ages; the geological significance (Wilson, 1989). Compared to the monzogranite, the tonalite samples of these three spots should be interpreted with caution. As shown in the have high Sr (479–617 ppm) contents, variable Y contents of 16.9–35.5 U/Yb versus Y discrimination diagram (Fig. 8B), the zircons from the ppm, K/Rb ratios of 214–307, variable Nb/Ta ratios of 8.27–24.61, and monzogranite and tonalite plotted in the transition zone between the oce- Ba/Th = 32.88–128.58. anic crust and continental crust (Grimes et al., 2007).

402 www.gsapubs.org | Volume 8 | Number 4 | LITHOSPHERE

TABLE.1 ANALYTICAL RESULTS OF MAJOR AND TRACE ELEMENTS (PPM) FROM THE MONZOGRANITE AND TONALITE FROM THE SHIHE PLUTON, SOUTHERN ZHANGGUANGCAI RANGE STH-3 STH-4 STH-5 STH-6 STH-7 STH-8 STH-2-1 STH-2-3 SHT-2-4 STH-2-5 STH-2-6 (%) Monzogranite Tonalite

SiO2 74.68 73.46 73.21 65.06 64.47 66.2567.39 67.6663.78 64.5764.90

TiO2 0.20 0.21 0.19 0.35 0.37 0.39 0.44 0.32 0.39 0.41 0.36

Al2O3 13.90 14.40 14.22 19.09 19.29 18.6317.18 17.8819.48 19.2019.34

Fe2O3T 1.44 1.46 1.47 2.42 2.43 2.33 3.33 2.32 2.75 2.59 2.53 MnO 0.06 0.07 0.06 0.08 0.09 0.09 0.12 0.07 0.08 0.09 0.09 MgO 0.41 0.44 0.41 0.69 0.74 0.65 0.83 0.65 0.79 0.73 0.70 CaO 1.21 1.38 1.34 3.12 3.27 2.88 2.88 3.07 3.37 3.18 3.18

Na2O 4.30 4.53 4.45 6.47 6.63 6.29 5.93 5.92 6.22 6.62 6.72

K2O 3.83 3.57 3.80 2.22 1.91 2.17 1.66 1.94 2.19 1.87 2.02

P2O5 0.06 0.06 0.07 0.11 0.110.100.130.100.100.110.11 LOI 0.31 0.84 0.30 0.55 0.47 0.47 0.36 0.48 0.69 0.39 0.32 Total 100.40 100.42 99.52 100.16 99.78 100.25 100.25 100.41 99.8499.76 100.27 Li 26.2 22.3 22.2 40.0 41.3 31.1 43.5 32.8 35.9 39.0 37.1 Be 2.71 3.20 2.39 3.05 3.21 3.07 2.76 3.01 3.04 2.87 2.93 Sc 3.72 3.75 3.47 4.29 4.62 3.83 6.89 2.95 3.37 4.59 4.47 V 16.1 15.3 16.4 22.7 20.7 14.6 29.5 18.3 20.5 18.3 17.9 Cr 2.25 2.45 1.13 3.01 1.63 1.02 3.06 5.52 2.83 1.53 1.34 Co 185 189 153 107 79.6 80.3 109 111 96.3 10373.8 Ni 0.80 1.29 0.73 1.26 1.110.591.633.660.760.790.64 Cu 1.00 1.10 1.44 1.15 1.22 1.17 1.30 1.14 1.15 1.13 1.20 Zn 26.6 27.6 26.1 44.2 44.2 41.1 61.8 43.3 48.8 48.2 46.4 Ga 15.4 15.6 15.8 20.3 20.6 19.1 20.1 18.8 19.8 20.5 20.6 Ge 1.45 1.45 1.46 1.39 1.41 1.37 1.41 1.33 1.42 1.40 1.40 Rb 89.7 100 91.6 64.4 58.6 58.7 63.3 68.1 75.0 58.9 59.5 Sr 176 203 203 536 567 571479 583617 580574 Y 18.0 16.4 16.6 16.9 18.2 18.2 28.2 18.1 17.1 23.7 24.5 Zr 114 90.7 110 375 395 429482 368370 438439 Nb 11.8 13.1 10.5 11.0 11.5 11.6 17.8 10.3 11.3 15.9 15.5 Cs 1.58 2.39 1.49 2.44 2.51 2.19 3.16 2.57 2.75 2.47 2.54 Ba 681 842 847 483 481 675509 628673 546563 La 19.3 21.6 27.7 27.4 34.4 33.1 50.2 29.6 33.1 36.0 33.4 Ce 38.7 42.9 54.0 49.8 62.7 57.9 95.2 53.2 57.8 65.3 60.0 Pr 4.20 4.66 5.79 5.43 6.67 6.25 10.2 5.75 6.20 6.92 6.55 Nd 14.9 16.3 20.3 18.9 23.2 21.8 35.1 20.0 21.4 24.1 22.5 Sm 2.79 2.95 3.42 3.03 3.57 3.27 5.53 3.09 3.10 3.77 3.63 Eu 0.62 0.70 0.70 1.12 1.20 1.26 1.13 1.25 1.33 1.28 1.26 Gd 2.75 2.75 3.04 2.77 3.12 2.98 4.99 2.82 2.73 3.67 3.62 Tb 0.41 0.40 0.43 0.39 0.43 0.42 0.70 0.40 0.38 0.54 0.54 Dy 2.64 2.48 2.60 2.49 2.70 2.69 4.40 2.59 2.45 3.53 3.59 Ho 0.55 0.51 0.52 0.53 0.57 0.58 0.91 0.57 0.54 0.77 0.80 Er 1.75 1.57 1.58 1.78 1.92 1.94 2.91 1.95 1.84 2.54 2.61 Tm 0.30 0.27 0.26 0.32 0.35 0.34 0.47 0.34 0.34 0.42 0.43 Yb 2.09 1.84 1.74 2.56 2.77 2.63 3.43 2.62 2.61 3.00 3.10 Lu 0.33 0.28 0.27 0.44 0.48 0.45 0.57 0.45 0.45 0.50 0.52 Hf 3.27 2.57 3.09 8.06 8.58 9.25 10.7 8.04 8.03 9.57 9.49 Ta 1.22 1.59 0.85 1.29 1.39 1.18 1.44 1.26 1.35 1.36 1.30 Pb 16.5 13.9 14.8 14.7 14.3 14.7 13.2 12.9 13.8 14.4 14.8 Th 8.33 8.72 10.4 6.99 8.47 7.19 15.5 7.32 7.46 9.22 8.53 U 1.80 1.72 1.44 1.37 1.72 1.41 2.46 1.81 1.64 1.71 1.74 Mg# 39.9 41.3 39.4 39.9 41.5 39.4 36.7 39.5 40.1 39.6 39.2 A/CNK 1.04 1.04 1.03 1.02 1.02 1.04 1.02 1.03 1.04 1.03 1.02 Eu* 0.68 0.75 0.66 1.18 1.10 1.23 0.66 1.30 1.40 1.05 1.06

(La/Yb)N 6.60 8.42 11.39 7.69 8.91 9.02 10.508.119.098.627.73 Nb/Ta 9.62 8.27 12.23 8.59 8.27 9.87 12.328.238.3211.70 11.93

Note: LOI —loss on ignition; A/CNK—Al2O3 /(CaO + Na2O + K2O).

LITHOSPHERE | Volume 8 | Number 4 | www.gsapubs.org 403

Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/8/4/396/3040314/396.pdf by guest on 27 September 2021 JIANG-FENG QIN ET AL.

(C)(Sr/Ce) (B)(Nb/K)N N (A)(Ba/Rb)N tonalite 1.00 monzogranite 0.40 0.80

0.80 0.30 0.60 0.60 0.20 0.40 0.40 0.10 0.20 0.20

compositional com 0.00

0.00 0.00 compos SiO% 63.0 68.0.0 73.0 SiO2% 63.0 68.073.0 2 63.0 68.0 773.0 SiO%2

(E)(Zr/Sm)N p (F)(Eu/Gd)N

(D)(P/Nd)N o 5.00 si 1.60 t 0.30 i t i o 4.00 1.20 iona na 0.20 l ga

ga 3.00 0.80 l ga p 0.10 2.00 p 0.40 p

1.00 0.00 0.00 SiO% 63.0 68.00 73.0 2 63.0 68.0 73.0 SiO2% 63.068.0773.0 SiO%2

(H)(Eu)N (I)(Ba)N (G)(Ti/Gd)N 8.00 118.0 0.40 7.00 108.0 0.30 6.00 98.0

0.20 5.00 88.0

0.10 4.00 78.0

3.00 68.0 0.00 8.00 13.0018.00 23.00 28.00 (Sr)N 8.00 13.00 18.0023.00 28.00 (Sr)N 63.0 68.0 73.0 SiO%2

Figure 5. Selected trace element ratios versus SiO2 or SrN (after Slaby and Martin, 2008) for monzogranite and tonalite from the Shihe pluton. Data are normalized to primitive mantle (Sun and McDonough, 1989).

TABLE 2. WHOLE-ROCK Sr-Nd ISOTOPIC COMPOSITION FOR THE MONZOGRANITE AND TONALITE FROM THE SHIHE PLUTON, ZHANGGUANGCAI RANGE

87 86 87 86 87 86 143 144 147 144 §143 144 Rock Samples Sr Rb Sr/ Sr 2sm Rb/ Sr* Sr/ Sr Nd Sm Nd/ Nd 2sm Sm/ Nd*TDM εNd(t) Nd/ Nd (ppm) (ppm) (200 Ma) (ppm) (ppm) (Ga)† (200 Ma) tonalite STH-2-3 583 68.1 0.705688 0.000006 0.338 0.704631 20.0 3.09 0.512585 0.000004 0.0930.751.9 0.512451 tonalite STH-2-5 580 58.9 0.705544 0.000006 0.294 0.704625 24.1 3.77 0.512658 0.000004 0.0950.653.3 0.512522 monzogranite STH-3 176 89.7 0.708721 0.000010 1.471 0.704118 14.9 2.79 0.512945 0.000024 0.113 0.30 8.30.512782 monzogranite STH-4 203 100 0.708676 0.000008 1.428 0.704207 16.3 2.95 0.513121 0.000022 0.1090.0511.70.512964 *87Rb/86Sr and 147Sm/144Nd ratios were calculated using Rb, Sr, Sm and Nd contents, measured by inductively coupled plasma–mass spectrometry. † 147 144 143 144 TDM (depleted mantle model age) values were calculated using present-day ( Sm/ Nd)DM = 0.2137 and ( Nd/ Nd)DM = 0.51315. § 147 144 143 144 εNd(t) values were calculated using present-day ( Sm/ Nd)CHUR = 0.1967 and ( Nd/ Nd)CHUR = 0.512638 (CHUR—chondritic uniform reservoir).

TABLE 3. WHOLE-ROCK Pb ISOTOPIC COMPOSITION FOR THE MONZOGRANITE AND TONALITE FROM THE SHIHE PLUTON, ZHANGGUANGCAI RANGE Rock type Sample UThPb 206Pb/204Pb 2σ 207Pb/204Pb 2σ 208Pb/204Pb 2σ 238U/204Pb* 232Th/204Pb 206Pb/204Pb 207Pb/204Pb 208Pb/204Pb (200 Ma)† (200 Ma)† (200 Ma)† tonalite STH-2-3 1.81 7.32 12.9 18.950 0.001 15.577 0.000 38.351 0.002 8.90 36.93 18.641 15.561 37.945 tonalite STH-2-5 1.71 9.22 14.4 18.663 0.001 15.568 0.000 38.415 0.001 7.54 41.60 18.401 15.555 37.958 monzogranite STH-3 1.80 8.33 16.5 18.701 0.001 15.574 0.001 38.327 0.002 6.87 32.68 18.463 15.562 37.968 monzogranite STH-4 1.72 8.72 13.9 18.797 0.000 15.572 0.000 38.371 0.001 7.83 40.61 18.525 15.558 37.924 *Calculated by measured whole-rock U, Th and Pb contents (see Table 1) and present-day whole-rock Pb isotopic ratios. †Initial Pb isotopic ratio at t = 200 Ma, calculated using single-stage model.

404 www.gsapubs.org | Volume 8 | Number 4 | LITHOSPHERE

1000.0 1000 A C

100.0 tle 100 n a e e m

10.0 10 imitiv r ck/Chondrit

o STH-3 R STH-3 STH-4 rock/p 1.0 STH-4 1.0 STH-5 STH-5 Upper continental crust,Rudnick&Gao,2003 Upper continental crust (Rudnick & Gao, 2003) Lower continental crust,Rudnick&Gao,2003 Lower continental crust (Rudnick & Gao, 2003) 0.1 0.1 Rb Ba Th UNbTaKLa Ce Pb Pr Sr PNdZrHfSmEuTiGdTbDyYHo Er Tm Yb Lu La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

1000.0 1000 B D e tl

100.0 n 100 a e m ve ti mi

10.0 i 10 r p / k c Rock/Chondrit ro 1.0 STH-6 STH-7 1.0 STH-8 STH-2-1 STH-6 STH-7 STH-2-3 STH-2-4 STH-8 STH-2-1 STH-2-5 STH-2-6 STH-2-3 STH-2-4 Lower continental crust (Rudnick & Gao, 2003) STH-2-5 STH-2-6 Lower continental crust (Rudnick & Gao, 2003) 0.1 La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu 0.1 Rb Ba Th UNbTaKLa Ce Pb Pr Sr PNdZrHfSmEuTiGdTbDyYHo Er Tm Yb Lu Figure 6. (A, B) Chondrite-normalized rare earth element patterns for monzogranite and tonalite from the Shihe pluton. (C, D) Primitive mantle–normalized trace element spider diagrams. Normalized values are from Sun and McDonough (1989).

DISCUSSIONS feldspar are the predominant minerals that host Eu and Sr in granitic melt (Rollinson, 1993; Slaby and Martin, 2008); considering the high

Significant Geochemical Variations between Monzogranite and BaN values in the monzogranite, we argue that the geochemical variation Tonalite: Implications for Two Distinct Source Regions between tonalite and monzogranite indicates that the tonalite has a more plagioclase component. This phenomenon indicates that normal frac- Geochemical variations are a common feature in granitic rocks, and the tional crystallization from a homogeneous source cannot account for the following models have been applied to explain the chemical variations in chemical variations between the tonalite and monzogranite. Furthermore, granitic rocks suites: (1) different partial melting conditions, resulting in the monzogranite samples display more depleted whole-rock Sr-Nd-Pb different melting reactions from a homogeneous source region; (2) two isotopic compositions and lower total REE contents (91.2–122.3 ppm),

distinct source regions; and (3) fractional crystallization and assimilation suggesting that assimilation of crustal rocks cannot result in higher SiO2,

of wall rocks (Pitcher, 1997). Clemens and Stevens (2012) argued that K2O, and Rb contents. Therefore, the geochemical variations between when granitic melts segregate from their source region, the melt may carry the tonalite and monzogranite indicate that they were derived from two small crystals of the peritectic phase assemblage formed in the melting distinct source regions. reaction, and this mechanism can be responsible for most of the primary elemental variations in granitic magmas. Monzogranite: Melting of MORB-Sediment Mélanges The tonalite and monzogranite from the Shihe area have identical formation ages but different geochemical features. The tonalite samples The geochemistry of granitic rocks provides us with windows into

display low SiO2 and K2O contents and high Al2O3, TiO2, CaO, and MgO the partial melting process and conditions and materials at unseen depths

contents, while the monzogranite samples have higher SiO2, K2O, and within the continents (Clemens, 2014). The monzogranite samples from

Rb contents and low TiO2, Fe2O3total, and MgO contents (Table 1). The the Shihe area display high SiO2 (73.21–74.68 wt%), K2O (3.57–3.83

tonalite and monzogranite thus have a distinct compositional gap (Fig. wt%), and Rb (89.7–100 ppm) contents and low Al2O3 contents (13.90–

5); the tonalite samples display higher (Ba/Rb)N, (Sr/Ce)N, EuN, SrN val- 14.40 wt%), with A/CNK values of 1.03–1.04, low Sr (176–203 ppm), ues than those of the monzogranite samples. Plagioclase and alkaline and high Rb/Sr (0.45–0.51) ratios, as well as significant negative Eu

LITHOSPHERE | Volume 8 | Number 4 | www.gsapubs.org 405

Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/8/4/396/3040314/396.pdf by guest on 27 September 2021 JIANG-FENG QIN ET AL.

10 400-179MaMORB A

adakites that derived newly underplated basaltic crust adakites that derived (Cordillera Blanca in south America and 5 from young oceanic Separation Point in New Zealand) crust

87 86 Figure 7. (A) ( Sr/ Sr)i versus eNd(t) for monzogranite 0 and tonalite from the Shihe pluton. MORB—mid- lithospheric mantle oceanic ridge basalt. (B) 208Pb/204Pb versus 206Pb/204Pb diagram (revised from Rollinson, 1993). (C) 207Pb/204Pb versus 206Pb/204Pb. Adakitic rocks directly derived from -5 a thick crust (lower crustal melting) are after Atherton Nd(t)

ε and Petford (1993) and Petford and Atherton (1996). Cenozoic subducted oceanic crust-derived adakites are after Defant (1990) and Sajona et al. (2000). 400– -10 179 Ma MORB is from Tribuzio et al. (2004) and Xu and Castillo (2004). Late Triassic igneous rocks from the northern margin of the North China craton are from Yang et al. (2007, 2012). Triassic volcanic rocks from -15 the eastern part of the Jilin-Heilongjiang province are from Xu et al. (2009). NHRL—Northern Hemisphere monzogranite Late- Triassic reference line (Th/U = 0.4); EM—enriched mantle; tonalite igneous rocks DM—depleted mantle; HIMU—high µ 238U/204Pb; BSE— -20 from the North late-Triassic volcanic rocks from Bulk silicate Earth. the eastern Heilongjiang province China Craton (Xu et al.,2009) -25 0.702 0.704 0.706 0.708 0.710

87 86 (Sr/ Sr)i

) ron upper crust 15.9 h EMII HIMU Ga HIMU C oc 5 B .5 Ge 4 41 ( a) HRL 7G N 15.7 BSE 7 Pb

b EMII 04 lower crust NHRL(1.

P 40 4 20 Pb / / roup 15.5 MORB b L g 20 72

P 39 A EMI? PREMA 08 DUP monzogranite 2 EMI tonalite Triassic volcanic rocks 15.3 38 DM (b) from the Zhangguangcai pacific MORB RangeS( hao et al.,2013) 16 21 37 17 18 19 20 22 Indian oecan 206204 MORB Pb/ Pb DM

17 18 19 20 21 206Pb/P204 b

anomalies of 0.62–0.70. As shown in the Rb/Sr versus Rb/Ba diagram However, the monzogranite samples display low SREE contents

(Fig. 9A), the monzogranite samples display high Rb/Sr and Rb/Ba ratios, (91.22–122.34 ppm) and (La/Yb)N ratios of 6.6–11.4, which indicate suggesting that they were derived from partial melting of graywackes the low content of accessory minerals in their source region (Bea, 1996;

(Sylvester, 1998). The biotites have high K2O and Rb, and low K/Rb Bea and Montero, 1999; Hoskin et al., 2000). Compared to the tonalite, ratios (Clemens, 2014), and the high K/Rb ratios (296–355) of the mon- the monzogranite samples display more depleted Sr-Nd isotopic com- 87 86 143 144 zogranite samples suggest that biotite is the predominant residue mineral positions: ( Sr/ Sr)i = 0.704118–0.704207, high Nd/ Nd ratios of

in their source region. In the Al2O3 + CaO + Na2O + K2O versus A/CNK 0.512905–0.512929, eNd(t) values of +8.3 to +11.7, and single-stage Nd 87 86 diagram (Fig. 9B), all the samples plot in the field of melts derived from model ages of 0.30–0.05 Ga, as shown in the ( Sr/ Sr)i-eNd(t) diagram graywackes (Patiño Douce, 1999). These geochemical features are iden- (Fig. 7A). The monzogranite samples display Sr-Nd isotopic compositions tical with the I-type granites that formed in the collisional orogenic belt identical to those of the Cenozoic adakite derived from young and hot (Chappell and White, 1992; Chappell et al., 2000). Calc-alkaline to high-K oceanic crust (Defant, 1990); zircons from the monzogranite also display calc-alkaline I-type granites are usually considered to have resulted from depleted Lu-Hf isotopic compositions (Fig. 8A), and all the grains display

partial melting of low to middle continental crust (Chappell and White, positive eHf(t) values of +7.8 to +18.2, with single-stage Hf model ages of 1992; Pitcher, 1997). 542–120 Ma. These features also suggest that the monzogranite samples

406 www.gsapubs.org | Volume 8 | Number 4 | LITHOSPHERE

LITHOSPHERE | Volume 8 | Number 4 | www.gsapubs.org 407

Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/8/4/396/3040314/396.pdf by guest on 27 September 2021 JIANG-FENG QIN ET AL.

20 100 monzogranite depe A tonalite B lted mantl a 10 e reworking of juvenile basaltic 1.0G 10 crust continental crust Chondrite zircon 0 t

reworking of a ncient continental Ga Crus crust 0 1.0 2. 5 U/Yb

Hf (t ) a -10 G 0.01 ε 5 f= 2. 7 H monzogranite 17 / tonalite a 6 Lu 17 0.1 -20 oceanic crust 3.0G zircon

-30 0.01 170 190 210 230 300 1000 2000 3000 10 100 1000 10000100000 crystallization ages(Ma) Y(ppm)

Figure 8. (A) Diagram of eHf(t) versus time for the zircons from monzogranite and tonalite. (B) U/Yb versus Y diagram (after Grimes et al., 2007). Dotted vertical line defines mixing line between a hypothetic Neoproterozoic juvenile crust and Paleoproterozoic continental crust.

100 35 Felsic pelites 1100 °C – 1.5 GPa A 1.6 B Greywacks C 30 0.4 1050 °C – 1.5 GPa Mafic pelites tonalite 1100 °C – 2.0 GPa O) calc-alkaline 10 monzogranite 2 h 1.4 granites 25 ric - s +K ay e 0.3 l c N C O r 2 0.4 sour 1.2 b) 20 Y y-poos 30% Na 1 la Rb/Ba C urce Calculated

o O+ s 60% peraluminous HP 15 0.3 0.2 G pelite-derived (Ce/ r

a t p metagraywacke melt 1 metaluminous r gneiss C e s 90% ( e 50%basalt 10 0.2 nt 0.1 Xs=1

Calculated O/ 0.1 23 0.75 Gr 0.8 t fre psammite- X=Grt 0.1 e

Shale Al derived melt 15%basalt LP 5 0.5 0.25 langes amphibolite Basalt Graywacke 0.6 Mé Xs=0MORB 0.01 0.20.3 0.4 0 05 10 15 20 25 30 0.11 10 100 Al23O+CaO+NaO22+K O Rb/Sr YbN Figure 9. (A) Rb/Sr versus Rb/Ba discrimination diagram (after Sylvester, 1998) for monzogranite and tonalite from the Shihe pluton. Blue circle— melts compositions derived from graywacke; blue square—melts compositions derived from psammite; blue triangle—melts compositions derived

from basalt. (B) Al2O3 + CaO + Na2O + K2O versus Al2O3/(CaO + Na2O + K2O) diagram (after Patiño Douce, 1999). HP—high pressure; LP—low pressure;

CA Grtes—calc-alkaline granites. (C) YbN versus (Ce/Yb)N diagram (after Castro et al., 2010). Blue circle—melts produced at temperature, T = 1100 °C, pressure, P = 1.5 GPa; gray star—melts produced at T = 1050 °C, P = 1.5 GPa; blue hexagon—melts produced at T = 1100 °C, P = 2.0 GPa; Xs—content of metagraywackes gneiss in mélanges. MORB—mid-oceanic ridge basalt.

were derived from a juvenile source region; like the zircons from the the mixture of basaltic rocks (MORB-derived amphibolite) and sedimen- tonalite, the zircons from the monzogranite also have transitional chemical tary components (biotite-rich metagraywacke) in the mantle wedge can features between oceanic crust zircon and continental crust zircon (Fig. produce Cordilleran-type granodioritic magmas. The depleted Sr-Nd- 8B). In summary, the monzogranite samples display some contradictory Hf isotopic compositions and low SREE contents of the monzogranite

geochemical features: their high SiO2, K2O, and Rb contents suggest the indicate that the primitive melts were derived from melting of juvenile sediment in their source region, but the depleted Sr-Nd-Hf isotopic com- basaltic rocks (MORB), and the subsequent mixing with granitic melts

positions and low SREE contents indicate a juvenile and depleted source derived from sedimentary rocks can account their high K2O and Rb con-

region. These contradictory geochemical features have also been found tents. Considering the high SiO2 contents and low Sr contents, it can be in Cordilleran-type batholiths (Wyllie, 1977) that formed in the active inferred that the primitive melts were formed by low-degree melting of continental margin. Castro et al. (2010) proposed an alternative view of basaltic rocks with plagioclase residue in the source region (Rapp and the genesis of Cordilleran-type batholiths; they argued that melting of Watson, 1995; Clemens, 2014). Overall, the monzogranite samples from

408 www.gsapubs.org | Volume 8 | Number 4 | LITHOSPHERE

the Shihe area display geochemical features identical to Cordilleran-type displaying some features of S-type granites (Chappell and White, 1974). In batholiths, i.e., the primitive trondhjemitic melts derived from juvenile summary, according to the geochemical features listed here, we argue that basaltic rocks mixed with the granitic melts derived from sedimentary the Early Jurassic tonalite from the Shihe area may have been formed by rocks formed the monzogranite. partial melting of Neoproterozoic juvenile basaltic crust in intermediate- to

high-pressure conditions. Their relatively low SiO2 contents (63.78–67.39 Na-rich Tonalite: Melts Derived from Juvenile Basaltic Crust wt%) also require temperatures >1000–1100 °C (Rapp and Watson, 1995).

The geochemistry of the granitic rocks was controlled by the tem- Early Mesozoic Tectonic Evolution of Zhangguangcai Range perature-pressure conditions of the source rocks, with or without the involvement of fluids during the partial melting process and subsequent The Mesozoic to Cenozoic westward subduction of the paleo–Pacific magmatic process, i.e., wall-rock assimilation, magma mixing, and frac- plate beneath the Eurasian continent caused significant geological phe- tional crystallization (Rapp and Watson, 1995; Pitcher, 1997; Brown, 2010, nomena in eastern China, i.e., widespread I-type granites and associated 2013). Experiments have revealed that partial melting of both oceanic volcanic rocks in northeastern China (Wu et al., 2002, 2011; Xu et al., and continental crust (including basaltic lower crust and granitic upper 2009, 2013; Zhou and Wilde, 2013; Wang et al., 2015; Guo et al., 2015), crust) can produce granitic melt (Brown, 2001, 2013; Castro et al., 2010). the Mesozoic decratonization process in the North China craton (Zhai et Therefore, the first step is to determine whether the granitic rocks were al., 2011), and Mesozoic granites and Cenozoic basalts in southeast China derived from oceanic crust or continental crust. (Zhou et al., 2006; He and Xu, 2012). In northeastern China, the initiation

The tonalite samples from the Shihe area display high Na2O/K2O ratios time and tectonic style of the paleo-Pacific subduction are controversial

of 2.84–3.57 and are characterized by high Na2O (5.92–6.72 wt%) and (Wu et al., 2011; Xu et al., 2013; Zhou and Wilde, 2013; Guo et al., 2015).

Al2O3 (17.18–19.34 wt%) contents, low K2O (1.66–2.22 wt%) contents, The Late Triassic to Early Jurassic (210–155 Ma) I-type granites in north- 87 86 and relatively depleted Sr-Nd isotopic compositions, with ( Sr/ Sr)i = eastern China were considered to result from the westward subduction 0.704625–0.704631 and 143Nd/144Nd ratios of 0.512572–0.512878, with of the paleo–Pacific plate (Wu et al., 2011). The Early Triassic (228–201

eNd(t) values of +1.9 to +3.3. These features are identical to the Na-rich Ma) bimodal igneous suites from the eastern Heilongjiang province also intermediate to silicic rocks from active continental margins (Defant, 1990; support the subduction of the paleo–Pacific plate beneath Eurasia (Wang Petford and Atherton, 1996; Petford and Gallagher, 2001). Na-rich ada- et al., 2015). However, the detailed subduction process and origin of the kitic rocks that formed in active continental margins are considered to subduction-related igneous rocks are still not well understood. Guo et al. result from partial melting of hot and young oceanic slabs (Kay, 1978; (2015) reported an Early Jurassic mafic intrusive complex from the Tumen Defant, 1990; Drummond et al., 1996) or melting of newly underplated area, and the detailed mineral chemistry and whole-rock geochemistry indi- basaltic crust (Petford and Atherton, 1996). Some have argued that partial cate that these mafic rocks crystallized in a water-saturated parental magma melting of mafic lower crust in postcollisional settings can also produce that was comparable to that of the arc mafic cumulates, in combination with Na-rich adakitic melts (Coldwell et al., 2011; Qian and Hermann, 2013). other north-south–trending mafic rocks and related I-type granites (Wu et Compared to the Triassic oceanic crust derived from a depleted astheno- al., 2011; Yu et al., 2012). Guo et al. (2015) also proposed Early Jurassic

sphere (White and Klein, 2014), the tonalite samples display lower eNd(t) subduction of the paleo–Pacific oceanic plate beneath northeastern China. values of +1.9 to +3.3, with corresponding model ages of 0.65–0.75 Ga, The monzogranite was considered to be derived from partial melting suggesting that they were derived from Neoproterozoic juvenile basaltic of MORB-sediment mélanges in the subduction zone, while the Na-rich crust. These features are consistent with other Mesozoic granites from the tonalite was formed by partial melting of juvenile basaltic crust in the Zhangguangcai Range (Guo et al., 2010; Wu et al., 2011). Furthermore, active continental margin. We propose that this Early Jurassic monzo- the tonalite samples have low to intermediate K/Rb ratios of 217–307, granite-tonalite association in the Shihe area was formed by the Early suggesting hornblende rather than biotite residue in their source region Jurassic westward subduction of the paleo–Pacific oceanic crust beneath

(Peacock et al., 1994). In combination with their high Al2O3/TiO2 and low northeastern China. In the case of oceanic subduction (Fig. 10), melting

CaO/Na2O ratios (Table 1), it can be inferred that there were limited sedi- of sediment in the subduction channel produces leucogranitic melts, and mentary rocks in their source region (Sylvester, 1998). Zircons from the these melts assimilate some basaltic rocks (i.e., oceanic crust in the sub- tonalite also display depleted Lu-Hf isotopic compositions (Table 4); some duction zone) and induce further melting of the basaltic rocks (Otamendi

grains even have eHf(t) values >+10. The corresponding single-stage model et al., 2009; Castro et al., 2010). Mixing between the leucogranitic melts ages are identical with the zircon U-Pb ages, suggesting depleted mantle and the melts derived from the oceanic crust formed the monzogranite

materials in their source region (Chauvel et al., 2008). The trace element samples that have high SiO2 contents and depleted Sr-Nd-Hf isotopic geochemistry of zircons has been applied to distinguish the zircons that compositions. In addition, melts or fluids derived from the subducted crystallized from continental or oceanic crust (Grimes et al., 2007); zir- crust induced partial melting of the basaltic rocks situated in the mantle cons from oceanic crust usually have higher Y contents and lower U/Yb wedge, and melts from these basaltic rocks formed the Na-rich tonalite ratios. As shown in Figure 8B, zircons from the tonalite mainly plot in the in the Shihe area (Fig. 10). transition zone between continental crust zircon and oceanic crust zircon. Compared to the typical Na-rich adakites from the subduction zone CONCLUSIONS (Kay, 1978; Defant, 1990; Drummond et al., 1996; Condie, 2005) and trondhjemite-tonalite-granodiorite suites from the Archean craton (Smith- 1. The Early Jurassic monzogranite and tonalite from the Shihe area ies and Champion, 2000; Moyen and Martin, 2012), the tonalite samples display nearly identical 206Pb/208U ages of 201 ± 2 (MSWD = 1.2, 2s) and from the Shihe area also have high Sr (479–617 ppm) and Ba (481–675 198 ± 3 Ma (MSWD = 3.2, 2s), respectively; these ages are contempo- ppm), low Y (17.1–28.2 ppm), and negligible Eu anomalies (Eu*/Eu = raneous with the volcanic rocks from the eastern Heilongjiang Province.

1.05–1.30). However, their lower (La/Yb)N, (Ce/Yb)N, and Dy/Yb ratios 2. The monzogranite samples display high SiO2, K2O, and Rb con- (Fig. 9C) suggest a hornblende rather than garnet source region (Foley tents, as well as depleted whole-rock Sr-Nd-Pb isotopic compositions,

et al., 2002). The tonalite samples also have A/CNK values of 1.02–1.04, i.e., eNd(t) = +8.3 to +11.7, with single-stage Nd model ages of 0.30–0.05

LITHOSPHERE | Volume 8 | Number 4 | www.gsapubs.org 409

Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/8/4/396/3040314/396.pdf by guest on 27 September 2021 JIANG-FENG QIN ET AL.

Zhangguangcai westward subduction of the Range sea level paleo-Pacific plate tonalite monzogranite MOHO bduction zone s in su ent m sedi Figure 10. Proposed model for he t genesis of the Early Jurassic monzogranite-tonalite association from southern part of Zhangguangcai continental crust tonalite-monzogranite Range (revised from Castro et al., 2010).

lithospheric mantle molten mélange

asthenosphere subducted oceanic crust

involvement of sediments partial molten mantle in subduction zone

Ga. Zircons from the monzogranite also have depleted Lu-Hf isotopic Chappell, B., and White, A., 1974, Two contrasting granite types: Pacific Geology, v. 8, p. 173–174. Chappell, B., and White, A., 1992, I-and S-type granites in the Lachlan Fold Belt: Royal Society compositions. These contradictory geochemical features suggest that the of Edinburgh Transactions, Earth Sciences, v. 83, p. 1–26, doi:10.1017 /S0263593300007720. monzogranite may be derived from melting of MORB-sediment mélanges Chappell, B.W., White, A.J.R., Williams, I.S., Wyborn, D., and Wyborn, L.A.I., 2000, Lachlan Fold in the subduction zone. Belt granites revisited: High- and low-temperature granites and their implications: Aus- tralian Journal of Earth Sciences, v. 47, p. 123–138, doi:10.1046 /j.1440 -0952.2000.00766.x. 3. The Na-rich tonalite samples display lower SiO2 and higher TiO2 Chauvel, C., Lewin, E., Carpentier, M., Arndt, N.T., and Marini, J.-C., 2008, Role of recycled contents and depleted zircon Lu-Hf isotopic compositions. Considering oceanic basalt and sediment in generating the Hf-Nd mantle array: Nature Geoscience, their relatively evolved Sr-Nd-Pb isotopic compositions, it can be con- v. 1, p. 64–67, doi:10.1038/ngeo.2007.51. Clemens, J.D., 2014, Element concentrations in granitic magmas: Ghosts of textures past: sidered that the tonalite was derived from juvenile basaltic crust in the Journal of the Geological Society [London], v. 171, p. 13–19, doi:10 .1144 /jgs2013 -008. active continental margin. Clemens, J.D., and Stevens, G., 2012, What controls chemical variation in granitic magmas?: 4. The Early Jurassic monzogranite-tonalite association from the Lithos, v. 134–135, p. 317–329, doi:10.1016/j.lithos.2012.01.001. Coldwell, B., Clemens, J., and Petford, N., 2011, Deep crustal melting in the Peruvian Andes: Shihe area was caused by westward subduction of the paleo–Pacific plate Felsic magma generation during delamination and uplift: Lithos, v. 125, p. 272–286, doi: beneath northeastern China. 10.1016/j.lithos.2011.02.011. Condie, K.C., 2005, TTGs and adakites: Are they both slab melts?: Lithos, v. 80, p. 33–44, doi: 10.1016/j.lithos.2003.11.001. ACKNOWLEDGMENTS Defant, M.J., 1990, Derivation of some modern arc magmas by melting of young subducted This work was supported by the Chinese Geological Survey (project 1212011121085), the Foun- lithosphere: Nature, v. 347, no. 6294, p. 662–665, doi:10 .1038 /347662a0. dation for the Author of National Excellent Doctoral Dissertation of the People’s Republic of DePaolo, D. J., 1981, A neodymium and strontium isotopic study of the Mesozoic calc-alkaline China (201324), the National Natural Science Foundation of China (41102037, 41190072), and granitic batholiths of the Sierra Nevada and Peninsular Ranges, California: Journal of the Ministry of Science and Technology (MOST) Special Fund from the State Key Laboratory Geophysical Research, v. 86, no. B11, p. 10,470–10,488, doi:10 .1029 /JB086iB11p10470. of Continental Dynamics, Northwest University. We thank Kurt Stuewe, Ewa Slaby, and an Drummond, M.S., Defant, M.J., and Kepezhinskas, P.K., 1996, Petrogenesis of slab-derived anonymous reviewer for their constructive comments and kind suggestions. trondhjemite-tonalite-dacite/adakite magmas: Royal Society of Edinburgh Transactions, Earth Sciences, v. 87, p. 205–215, doi:10.1017 /S0263593300006611. REFERENCES CITED Foley, S., Tiepolo, M., and Vannucci, R., 2002, Growth of early continental crust controlled by melting of amphibolite in subduction zones: Nature, v. 417, no. 6891, p. 837–840, doi: Andersen, T., 2002, Correction of common lead in U-Pb analyses that do not report 204Pb: 10.1038/nature00799. Chemical Geology, v. 192, p. 59–79, doi:10 .1016 /S0009 -2541(02)00195-X. Atherton, M.P., and Petford, N., 1993, Generation of sodium-rich magmas from newly under- Griffin, W.L., Pearson, N.J., Belousova, E.A., and Saeed, A., 2006, Comment: Hf-isotope het- plated basaltic crust: Nature, v. 362, p. 144–146, doi: 10.1038 /362144a0. erogeneity in zircon 91500: Chemical Geology, v. 233, p. 358–363, doi:10 .1016 /j .chemgeo Bea, F., 1996, Residence of REE, Y, Th and U in granites and crustal protoliths: Implications .2006.03.007. for the chemistry of crustal melts: Journal of Petrology, v. 37, p. 521–552, doi:10.1093 Grimes, C.B., John, B.E., Kelemen, P.B., Mazdab, F.K., Wooden, J.L., Cheadle, M.J., Hanghøj, K., /petrology/37.3.521. and Schwartz, J.J., 2007, Trace element chemistry of zircons from oceanic crust: A method for Bea, F., and Montero, P., 1999, Behavior of accessory phases and redistribution of Zr, REE, Y, distinguishing detrital zircon provenance: Geology, v. 35, p. 643–646, doi:10 .1130 /G23603A.1. Th, and U during metamorphism and partial melting of metapelites in the lower crust: Guo, F., Fan, W., Gao, X., Li, C., Miao, L., Zhao, L., and Li, H., 2010, Sr-Nd-Pb isotope map- An example from the Kinzigite Formation of Ivrea-Verbano, NW Italy: Geochimica et ping of Mesozoic igneous rocks in NE China: Constraints on tectonic framework and Cosmochimica Acta, v. 63, p. 1133–1153, doi:10.1016/S0016-7037(98)00292-0. Phanerozoic crustal growth: Lithos, v. 120, p. 563–578, doi:10 .1016 /j .lithos.2010 .09 .020. Blichert-Toft, J., 2008, The Hf isotopic composition of zircon reference material 91500: Chemi- Guo, F., Li, H., Fan, W., Li, J., Zhao, L., Huang, M., and Xu, W., 2015, Early Jurassic subduction cal Geology, v. 253, p. 252–257, doi:10.1016/j.chemgeo.2008.05.014. of the Paleo-Pacific Ocean in NE China: Petrologic and geochemical evidence from the Tu- Brown, M., 2001, Orogeny, migmatites and leucogranites: A review: Journal of Earth System men mafic intrusive complex: Lithos, v. 224–225, p. 46–60, doi:10 .1016 /j .lithos .2015 .02 .014. Science, v. 110, p. 313–336, doi:10.1007 /BF02702898. Han, B.-F., Wang, S.-G., Jahn, B.-M., Hong, D.-W., Kagami, H., and Sun, Y.-L., 1997, Depleted- Brown, M., 2010, Melting of the continental crust during orogenesis: The thermal, rheological, mantle source for the Ulungur River A-type granites from North Xinjiang, China: Geo- and compositional consequences of melt transport from lower to upper continental crust: chemistry and Nd-Sr isotopic evidence, and implications for Phanerozoic crustal growth: Canadian Journal of Earth Sciences, v. 47, p. 655–694, doi:10.1139 /E09 -057. Chemical Geology, v. 138, p. 135–159, doi:10.1016/S0009-2541(97)00003-X. Brown, M., 2013, Granite: From genesis to emplacement: Geological Society of America Bul- He, Z.-Y., and Xu, X.-S., 2012, Petrogenesis of the late Yanshanian mantle-derived intrusions letin, v. 125, no. 7–8, p. 1079–1113, doi:10.1130 /B30877 .1. in southeastern China: Response to the geodynamics of paleo-Pacific plate subduction: Castro, A., Gerya, T., García-Casco, A., Fernández, C., Díaz-Alvarado, J., Moreno-Ventas, I., and Chemical Geology, v. 328, p. 208–221, doi:10.1016/j.chemgeo.2011.09.014. Löw, I., 2010, Melting relations of MORB–sediment mélanges in underplated mantle Hoskin, P.W.O., Kinny, P.D., Wyborn, D., and Chappell, B.W., 2000, Identifying accessory mineral wedge plumes: Implications for the origin of cordilleran-type batholiths: Journal of saturation during differentiation in granitoid magmas: An integrated approach: Journal Petrology, v.51, p. 1267–1295, doi: 10.1093 /petrology /egq019. of Petrology, v. 41, p. 1365–1396, doi:10.1093/petrology/41.9.1365.

410 www.gsapubs.org | Volume 8 | Number 4 | LITHOSPHERE

Iizuka, T., and Hirata, T., 2005, Improvements of precision and accuracy in situ Hf isotope mi- of the paleo-Pacific plate beneath Eurasia: Journal of Asian Earth Sciences, v. 97, p. croanalysis of zircon using the laser ablation–MC–ICPMS technique: Chemical Geology, 406–423, doi:10.1016/j.jseaes.2014.05.025. v. 220, p. 121–137, doi:10.1016/j.chemgeo.2005.03.010. White, W.M., and Klein, E.M., 2014, Composition of the oceanic crust, in Rudnick, R.L., ed., The Jahn, B.-M., 2010, Accretionary orogen and evolution of the Japanese Islands: Implications crust: Treatise on Geochemistry 4 (second edition): Oxford, Elsevier, p. 457–496, doi:10 from a Sr-Nd isotopic study of the Phanerozoic granitoids from SW Japan: American .1016/B978-0-08-095975-7.00315-6. Journal of Science, v. 310, p. 1210–1249, doi:10.2475 /10.2010 .02. Wilde, S.A., Zhang, X., and Wu, F., 2000, Extension of a newly identified 500 Ma metamor- Jahn, B.M., Griffin, W.L., and Windley, B., 2000, Continental growth in the Phanerozoic: Evidence phic terrane in north east China: Further U-Pb SHRIMP dating of the Mashan Complex, from Central Asia: Tectonophysics, v. 328, p. vii–x, doi:10 .1016 /S0040 -1951 (00) 00174-8. Heilongjiang Province, China: Tectonophysics, v. 328, p. 115–130, doi:10.1016/S0040 Kay, R.W., 1978, Aleutian magnesian andesites: Melts from subducted Pacific ocean crust: -1951(00)00180-3. Journal of Volcanology and Geothermal Research, v. 4, p. 117–132, doi:10 .1016/0377 Wilson, B.M., 1989, Igneous petrogenesis a global tectonic approach: Netherlands, Springer, -0273(78)90032-X. 466 p., doi:10.1007/978-1-4020-6788-4 Li, J.Y., 2006, Permian geodynamic setting of northeast China and adjacent regions: Closure Wu, F.-Y., Jahn, B.-M., Wilde, S., and Sun, D.-Y., 2000, Phanerozoic crustal growth: U-Pb and of the paleo-Asian Ocean and subduction of the paleo-Pacific Plate: Journal of Asian Sr-Nd isotopic evidence from the granites in northeastern China: Tectonophysics, v. 328, Earth Sciences, v. 26, p. 207–224, doi:10.1016/j.jseaes.2005.09.001. p. 89–113, doi:10.1016/S0040-1951(00)00179-7. Ludwig, K.R., 2003, ISOPLOT 3.0: A geochronological toolkit for Microsoft Excel: Berkeley Wu, F.-Y., Sun, D.-Y., Li, H., Jahn, B.-M., and Wilde, S., 2002, A-type granites in northeastern Geochronology Center Special Publication 4. China: Age and geochemical constraints on their petrogenesis: Chemical Geology, v. 187, Moyen, J.-F., and Martin, H., 2012, Forty years of TTG research: Lithos, v. 148, p. 312–336, doi: p. 143–173, doi:10.1016/S0009-2541(02)00018-9. 10.1016/j.lithos.2012.06.010. Wu, F.-Y., Jahn, B.-M., Wilde, S.A., Lo, C.-H., Yui, T.-F., Lin, Q., Ge, W.-C., and Sun, D.-Y., 2003, Otamendi, J.E., Ducea, M.N., Tibaldi, A.M., Bergantz, G.W., de la Rosa, J.D. and Vujovich, G.I., Highly fractionated I-type granites in NE China (I): Geochronology and petrogenesis: 2009, Generation of tonalitic and dioritic magmas by coupled partial melting of gab- Lithos, v. 66, p. 241–273, doi:10.1016/S0024-4937(02)00222-0. broic and metasedimentary rocks within the deep crust of the Famatinian magmatic Wu, F.-Y., Sun, D.-Y., Ge, W.-C., Zhang, Y.-B., Grant, M.L., Wilde, S.A., and Jahn, B.-M., 2011, arc, Argentina: Journal of Petrology, v. 50, p. 841–873, doi:10.1093 /petrology /egp022. Geochronology of the Phanerozoic granitoids in northeastern China: Journal of Asian Patiño Douce, A.E., 1999, What do experiments tell us about the relative contributions of crust Earth Sciences, v. 41, p. 1–30, doi:10.1016/j.jseaes.2010.11.014. and mantle to the origin of granitic magmas?, in Castro, A., et al., eds., Understanding Wyllie, P.J., 1977, Crustal anatexis: An experimental review: Tectonophysics, v. 43, p. 41–71, granites: Integrating new and classical techniques: Geological Society, London, Special doi:10.1016/0040-1951(77)90005-1. Publication 168, p. 55–75, doi:10.1144/GSL.SP.1999.168.01.05. Xu, J.F., and Castillo, P.R., 2004, Geochemical and Nd-Pb isotopic characteristics of the Tethyan Peacock, S.M., Rushmer, T., and Thompson, A.B., 1994, Partial melting of subducting oceanic asthenosphere: Implications for the origin of the Indian Ocean mantle domain: Tectono- crust: Earth and Planetary Science Letters, v. 121, p. 227–244, doi:10.1016/0012-821X physics, v. 393, p. 9–27, doi:10.1016/j.tecto.2004.07.028. (94)90042-6. Xu, W.-L., Ji, W.-Q., Pei, F.-P., Meng, E., Yu, Y., Yang, D.-B., and Zhang, X., 2009, Triassic volca- Pei, F.-P., Xu, W.-L., Yang, D.-B., Yu, Y., Meng, E., and Zhao, Q.-G., 2011, Petrogenesis of late nism in eastern Heilongjiang and Jilin provinces, NE China: Chronology, geochemistry, Mesozoic granitoids in southern Jilin province, northeastern China: Geochronologi- and tectonic implications: Journal of Asian Earth Sciences, v. 34, p. 392–402, doi:10 cal, geochemical, and Sr-Nd-Pb isotopic evidence: Lithos, v. 125, p. 27–39, doi:10.1016 .1016/j.jseaes.2008.07.001. /j.lithos.2011.01.004. Xu, W.-L., Pei, F.-P., Wang, F., Meng, E., Ji, W.-Q., Yang, D.-B., and Wang, W., 2013, Spatial- Petford, N., and Atherton, M., 1996, Na-rich partial melts from newly underplated basaltic temporal relationships of Mesozoic volcanic rocks in NE China: Constraints on tectonic crust: The Cordillera Blanca Batholith, Peru: Journal of Petrology, v. 37, p. 1491–1521, overprinting and transformations between multiple tectonic regimes: Journal of Asian doi:10.1093/petrology/37.6.1491. Earth Sciences, v. 74, p. 167–193, doi:10.1016/j.jseaes.2013.04.003. Petford, N., and Gallagher, K., 2001, Partial melting of mafic (amphibolitic) lower crust by Yang, J.-H., Sun, J.-F., Chen, F., Wilde, S.A., and Wu, F.-Y., 2007, Sources and petrogenesis of periodic influx of basaltic magma: Earth and Planetary Science Letters, v. 193, p. 483–499, Late Triassic dolerite dikes in the Liaodong Peninsula: Implications for post-collisional doi:10.1016/S0012-821X(01)00481-2. lithosphere thinning of the eastern North China Craton: Journal of Petrology, v. 48, Pitcher, W.S., 1997, The nature and origin of granite (second edition): Netherlands, Springer p. 1973–1997, doi:10.1093/petrology/egm046. Science & Business Media, 387 p., doi:10.1007/978-94-011-5832-9. Yang, J.-H., Sun, J.-F., Zhang, J.-H., and Wilde, S.A., 2012, Petrogenesis of Late Triassic intru- Qian, Q., and Hermann, J., 2013, Partial melting of lower crust at 10–15 kbar: Constraints on sive rocks in the northern Liaodong Peninsula related to decratonization of the North adakite and TTG formation: Contributions to Mineralogy and Petrology, v. 165, p. 1195– China Craton: Zircon U-Pb age and Hf-O isotope evidence: Lithos, v. 153, p. 108–128, 1224, doi:10.1007/s00410-013-0854-9. doi:10.1016/j.lithos.2012.06.023. Rapp, R.P., and Watson, E.B., 1995, Dehydration melting of metabasalt at 8–32 kbar: Impli- Yu, J.-J., Wang, F., Xu, W.-L., Gao, F.-H., and Pei, F.-P., 2012, Early Jurassic mafic magmatism in cations for continental growth and crust-mantle recycling: Journal of Petrology, v. 36, the Lesser Xing’an–Zhangguangcai Range, NE China, and its tectonic implications: Con- p. 891–931, doi:10.1093/petrology/36.4.891. straints from zircon U-Pb chronology and geochemistry: Lithos, v. 142–143, p. 256–266, Rudnick, R.L., and Gao, S., 2003, 3.01: Composition of the Continental Crust A2, in Holland, doi:10.1016/j.lithos.2012.03.016. H.D. and Turekian, K.K., eds., Treatise on Geochemistry, v. 3: Pergamon, Oxford, p. 1–64, Yuan, H.L., Gao, S., Liu, X.M., Li, H.M., Gunther, D., and Wu, F.Y., 2004, Accurate U-Pb age and doi:10.1016/B0-08-043751-6/03016-4. trace element determinations of zircon by laser ablation–inductively coupled plasma Rollinson, H., 1993, Using geochemical data: Evaluation, presentation, interpretation: Lon- mass spectrometry: Geostandards and Geoanalytical Research, v. 28, p. 353–370, doi: don, Longman, 352 p. 10.1111/j.1751-908X.2004.tb00755.x. Sajona, F.G., Maury, R.C., Prouteau, G., Cotten, J., Schiano, P., Bellon, H., and Fontaine, L., Yuan, H.-L., Gao, S., Dai, M.-N., Zong, C.-L., Günther, D., Fontaine, G.H., Liu, X.-M., and Diwu, 2000, Slab melt as metasomatic agent in island arc magma mantle sources, Negros C., 2008, Simultaneous determinations of U-Pb age, Hf isotopes and trace element com- and Batan (Philippines): Island Arc, v. 9, p. 472–486. positions of zircon by excimer laser-ablation quadrupole and multiple-collector ICP-MS: S¸engör, A.M.C., Natal’in, B.A., and Burtman, V.S., 1993, Evolution of the Altaid tectonic collage Chemical Geology, v. 247, p. 100–118, doi:10.1016/j.chemgeo.2007.10.003. and Palaeozoic crustal growth in Eurasia: Nature, v. 364, p. 299–307, doi:10 .1038 /364299a0. Zhai, M.-G., Santosh, M., and Zhang, L., 2011, Precambrian geology and tectonic evolution Shao, J.A., Li, Y., and Tang, K., 2013, Restoration of the orogenic processes of Zhuangguangcai of the North China Craton: Gondwana Research, v. 20, p. 1–5. doi: http://dx.doi.org/10 Range: Acta Petrologica Sinica, v. 29, p. 2959–2970. .1016/j.gr.2011.04.004. Słaby, E., and Martin, H., 2008, Mafic and felsic magma interaction in granites: The Hercynian Zhou, J.-B., and Wilde, S.A., 2013, The crustal accretion history and tectonic evolution of Karkonosze pluton (Sudetes, Bohemian Massif): Journal of Petrology, v. 49, p. 353–391, the NE China segment of the Central Asian Orogenic Belt: Gondwana Research, v. 23, doi:10.1093/petrology/egm085. p. 1365–1377, doi:10.1016/j.gr.2012.05.012. Smithies, R.H., and Champion, D.C., 2000, The Archaean high-Mg diorite suite: Links to tonal- Zhou, J.-B., Wilde, S.A., Zhang, X.-Z., Zhao, G.-C., Zheng, C.-Q., Wang, Y.-J., and Zhang, X.-H., ite-trondhjemite-granodiorite magmatism and implications for early Archaean crustal 2009, The onset of Pacific margin accretion in NE China: Evidence from the Heilongji- growth: Journal of Petrology, v. 41, p. 1653–1671, doi:10.1093 /petrology /41.12.1653. ang high-pressure metamorphic belt: Tectonophysics, v. 478, p. 230–246, doi:10 .1016 Sun, S.-S., and McDonough, W.F., 1989, Chemical and isotopic systematics of oceanic basalts: /j.tecto.2009.08.009. Implications for mantle composition and processes: Geological Society, London, Special Zhou, X.M., Sun, T., Shen, W.Z., Shu, L.S., and Niu, Y.L., 2006, Petrogenesis of Mesozoic gran- Publication 42, p. 313–345, doi:10.1144/GSL.SP.1989.042.01.19. itoids and volcanic rocks in South China: A response to tectonic evolution: Episodes, Sylvester, P.J., 1998, Post-collisional strongly peraluminous granites: Lithos, v. 45, p. 29–44, v. 29, p. 26–33. doi:10.1016/S0024-4937(98)00024-3. Tribuzio, R., Thirlwall, M.F., and Vannucci, R., 2004, Origin of the Gabbro–Peridotite Association MANUSCRIPT RECEIVED 12 NOVEMBER 2015 from the Northern Apennine Ophiolites (Italy): Journal of Petrology, v. 45, p. 1109–1124, REVISED MANUSCRIPT RECEIVED 20 APRIL 2016 doi: 10.1093/petrology/egh006. MANUSCRIPT ACCEPTED 17 MAY 2016 Wang, F., Xu, W.-L., Xu, Y.-G., Gao, F.-H., and Ge, W.-C., 2015, Late Triassic bimodal igneous rocks in eastern Heilongjiang Province, NE China: Implications for the initiation of subduction Printed in the USA

LITHOSPHERE | Volume 8 | Number 4 | www.gsapubs.org 411

Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/8/4/396/3040314/396.pdf by guest on 27 September 2021