Lithos 177 (2013) 352–365

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Spatial and temporal distribution of Mesozoic adakitic rocks along theTan-Lu fault, Eastern China: Constraints on the initiation oflithospheric thinning

Hai-Ou Gu a, Yilin Xiao a,⁎, M. Santosh b,c, Wang-Ye Li a, Xiaoyong Yang a, Andreas Pack d, Zhenhui Hou a

a CAS Key Laboratory of Crust–Mantle Materials and Environments, School of Earth and Space Sciences, University of Science and Technology of China, Hefei 230026, Anhui, Chinab School of Earth Science and Resources, China University of Geosciences, 29 Xueyuan Road, Beijing, 100083, PR Chinac Faculty of Science, Kochi University, Kochi 780-8520, Japand Georg-August-Universität, Geowissenschaftliches Zentrum, Abteilung Isotopengeologie, Goldschmidtstraße 1, 37077 Göttingen, Germany

⁎ Corresponding author.E-mail address: ylxiao@ustc.edu.cn (Y. Xiao).

0024-4937/$ – see front matter © 2013 Elsevier B.V. All rihttp://dx.doi.org/10.1016/j.lithos.2013.07.011

a b s t r a c t

a r t i c l e i n f o

Article history:Received 26 December 2012Accepted 9 July 2013Available online 17 July 2013

Keywords:AdakiteNorth China CratonThe Tan-Lu faultZircon U-Pb geochronologyOxygen isotope

TheMesozoic tectonics in East China is characterized by significant lithospheric thinning of the North China Cra-ton, large-scale strike-slip movement along the Tan-Lu fault, and regional magmatism with associatedmetallogeny. Here we address the possible connections between these three events through a systematic inves-tigation of the geochemistry, zircon geochronology and whole rock oxygen isotopes of the Mesozoic magmaticrocks distributed along the Tan-Lu fault in the Shandong province.The characteristic spatial and temporal distributions of high-Mg adakitic rocks along the Tan-Lu fault with em-placement ages of 134-128 Ma suggest a strong structural control for the emplacement of these intrusions,with magma generation possibly associated with the subduction of the Pacific plate in the early Cretaceous.The low-Mg adakitic rocks (127–120 Ma) in the Su-Lu orogenic belt were formed later than the high-Mg adakiticrocks, whereas in the Dabie orogenic belt, most of the low-Mg adakitic rocks (143-129 Ma) were generated ear-lier than the high-Mg adakitic rocks. Based on available data, we suggest that the large scale strike-slip tectonicsof the Tan-Lu fault in the Mesozoic initiated cratonic destruction at the south-eastern margin of the North ChinaCraton, significantly affecting the lower continental crust within areas near the fault. This process resulted incrustal fragments sinking into the asthenosphere and reacting with peridotites, which increased the Mg# ofthe adakitic melts, generating the high-Mg adakitic rocks. The gravitationally unstable lower continental crustbelow the Tan-Lu fault in the Su-Lu orogenic belt triggered larger volume delamination of the lower continentalcrust or foundering of the root.

© 2013 Elsevier B.V. All rights reserved.

1. Introduction

Adakites (or adakitic rocks) are originally suggested to be productsof melting of young and hot oceanic crust in subduction-zones (Defantand Drummond, 1990; Kay, 1978; Martin, 1999; Peacock et al., 1994;Pepiper andPiper, 1994; Stern andKilian, 1996). Geochemically, adakitesare characterized by high Sr, Al, and Na contents along with high Sr/Yand H/LREE (Heavy/Light Rare Earth Elements, (La/Yb)N for instance)ratios, implying a garnet-amphibolite or eclogite source without signif-icant amount of plagioclases in the residue (Rapp et al., 1991). Adakiticrocks of different ages have been reported from a number of terraneswithin different tectonic settings (e.g., Eyuboglu et al., 2011a,b, 2012;Guan et al., 2012; Yu et al., 2012). Adakitic features can also be gener-ated in some non-arc regions, through either the AFC (Assimilation–Fractional-Crystallization) process or partial melting of thickened ordelaminated lower crust (Castillo et al., 1999; Gao et al., 2004, 2006;

ghts reserved.

He et al., 2011; Huang et al., 2008; Liu et al., 2009; Meng and Zhang,2000; Wang et al., 2006a,b, 2007, 2010; Xu et al., 2002, 2008; Zhanget al., 2010). Experimental studies have also shown that adakitic meltscan be generated at pressures of ~1.2 GPa (i.e. a crustal thickness ofN40 km) through partial melting of mafic components (Rapp andWatson, 1995; Rapp et al., 1999; Xiong et al., 2011). Several examplesof non-arc adakitic rocks linkedwith crustal thickening or eclogitizationhave also been described, such as from continent–continent collisionbelts (He et al., 2011; Wang et al., 2007; Yang et al., 2005; Zhang et al.,2002, 2010), intracontinental settings (Gao et al., 2004, 2006; Huanget al., 2008; Liu et al., 2009; Liu et al., 2012; Xu et al., 2008; Zi et al.,2007) or active continental settings (Atherton and Petford, 1993; Kayand Kay, 2002).

The North China Craton (NCC) is a classic region to study cratonicdestruction because of the widespread lithospheric thinning belowthis craton during the late Jurassic to late Cretaceous (Cheng et al.,2013; Fan et al., 2000; Gao et al., 2002; Li et al., 2013; Menzies et al.,2007; Xu et al., 2013; Yang et al., 2012b; Zhai and Santosh, 2011,2013; Zhang, 2012; Zhang et al., 2002, 2003a). The several models

353H.-O. Gu et al. / Lithos 177 (2013) 352–365

proposed for the decratonization of the NCC include foundering of thelower continental crust (LCC) (Deng et al., 2007; Gao et al., 2004), ex-tension or thermal/chemical erosion of deep lithosphere (Xu, 2001),and hydration of lithosphere mantle (Chen et al., 2004; Niu, 2005). Ex-tensivemagmatism and associatedmetallogeny accompanied the litho-spheric thinning of the NCC in the Mesozoic, among which adakiticrocks constitute an important suite (Gao et al., 2006; Guo et al., 2013;Li et al., 2013; Xiong et al., 2011; Xu et al., 2006b, 2008; Yang et al.,2008; Zhai and Santosh, 2013). Notably, during the late-Jurassic toearly-Cretaceous, the Tan-Lu Fault witnessed large-scale strike-slip,which offset the Dabie and Su-Lu orogen belts for N550 km (Wang,2006; Zhang et al., 2003b). Although some previous studies have postu-lated some connections between the Tan-Lu fault and the near-faultadakitic rocks (Huang et al., 2008), the data reported so farwere focusedon the southern part of the Tan-Lu fault, with limited information fromthe Shandong region. The tectonic relationship between the fault andthe Dabie–Sulu orogenic belt is important in understanding the evolu-tion of the lithosphere under Eastern China. The adakitic magmatismin Shandong Province which is located in the central-northern part ofthe Tan-Lu fault is therefore of prime importance.

In this paper, we present whole rock elemental and oxygen isotopiccompositions, as well as zircon U–Pb ages for the Mesozoic magmaticrocks along the Tan-Lu fault in Shandong province. The results demon-strate that the high-Mg adakitic rocks with ages of 134–128 Ma occurwithin a zone that is parallel to the strike of the Tan-Lu fault. Our resultssuggest that the large-scale strike of the Tan-Lu fault in the Mesozoicmight have initiated the extensive lithospheric thinning of the south-east margin of the NCC.

2. Geological background and samples

The NCC had a prolonged evolution history during the early Precam-brianwithfinal cratonization during Paleoproterozoic (Zhai and Santosh,2011). The tectonic framework of this craton is mainly composed of theEastern Block, Western Block and the Central Orogenic Belt (also knownas the Trans-North China Orogen) (Santosh, 2010; Zhao, 2001). Large-scale Mesozoic magmatism and related mineralization characterize theEastern Block and the Central Orogenic Belt (e.g., Guo et al., 2013; Liet al., 2013 ,Yang et al., 2013).

The Western Block is made up of a thick crust (~45 km; Li et al.,2006; Zhao et al., 2001) and is underlain by a thick lithosphere(N150 km; Chen, 2010; Tian et al., 2009). The region is characterizedby relatively low surface heat flow (50–60 mW/m2; Hu et al., 2000).Only minor Phanerozoic volcanism and rare seismicity are recordedwithin this block. The Western Block is a composite amalgam of theYinshan Block in the north and the Ordos Block in the south, separatedby a Paleoproterozoic subduction-accretion-collision belt termed as theInner Mongolia Suture Zone (Santosh, 2010). A Khondalite Belt of highgrade granulite facies metapelites occurs within this suture zone, pre-serving evidence for ultrahigh-temperature metamorphism (Kuskyand Li, 2003; Liu et al., 2011; Santosh et al., 2007a,b, 2012; Wan et al.,2006a,b; Yin et al., 2009; Zhang, 2012; Zhao et al., 2005).

In contrast, the Precambrian crust in the Eastern Block and the un-derlying lithosphere are both relatively thin (a crust with 30–40 kmthickness and a lithosphere of b100 km; Chen, 2010; Li et al., 2006;Tian et al., 2009). Investigations on xenolithic peridotites in this blocksuggest a relatively cold, thick and refractory lithospheric mantle in Pa-leozoic, which was replaced by a fertile and hot lithospheric mantle inthe Cenozoic (Chu et al., 2009; Gao et al., 2002; Griffin et al., 1998;Menzies et al., 1993; Rudnick et al., 2004; Wu et al., 2006).

The Shandong province is located in the southeastern margin of theNCC and is subdivided into two parts by the Tan-Lu fault, the Luxi to thewest and the Jiaodong to the east. The Jiaodong terrane is attached tothe Su-Lu orogenic belt along the Wulian–Muping fault. The samplesfor this study were collected along the Tan-Lu Fault (Fig. 1), from theJiaodong and Luxi regions and the Su-Lu orogenic belt. Most of our

samples are intermediate-felsic intrusive rocks, covering two East–West profiles that cross the Tan-Lu fault and two North–South profilesparallel to the strike of the fault with a large spatial distribution (Fig. 1).

3. Analytical methods

57 rock samples were analyzed for whole rock element concentra-tions and oxygen isotopes with at least two samples of the intrusivesfrom each locality. 17 samples were selected for LA-ICP-MS zircon agedating. Also, 19 samples were selected for Sr–Nd isotope analysis.

3.1. Major and trace element geochemistry

Whole rock major elements and some trace elements were mea-sured by X-ray fluorescence (XRF) with a Philips PW 1480 automatedsequential spectrometer at the University of Göttingen. Glass beadswere fused with lithium tetraborate using procedures described inXiao et al. (2011). Trace elements of whole rocks were analyzed byICP-MS solution analyses. Rock powders were dissolved with HF,HClO4 and HNO3 in Teflon containers for over 48 h at 190 °C. Measure-mentswere conducted on an Elan 6100 DRC ICP-MS at the CAS Key Lab-oratory of Crust–Mantle Materials and Environments, University ofScience and Technology of China, Hefei (USTC).

3.2. Whole rock oxygen isotopes

Whole rock oxygen isotopes were analyzed at the University ofGöttingen, by means of infrared laser fluorination in combination withGC-CF-IRMMS (Gas Chromatography and Continuous Flow IsotopeRatioMonitoring gasMass Spectrometry). About 1.5 mgof rock powderwas loaded into an 18-pit Ni sample holder. After evacuation andheating the sample chamber to ~70 °C overnight (N12 h), materialswere reacted with purified F2 in a ~25 to ~30 mbar atmosphere, andheated with a CO2-laser at the energy of 50 W. The oxygenwas purifiedand injected via an open split valve of the GasBench II into the source ofa ThermoMAT253 gasmass spectrometer. The analytical error based onreplicate analysis and standard is better than 0.2‰ (2 sigma, for moredetails, see Gehler et al., 2011; Hofmann et al., 2012).

3.3. Dating zircon U–Pb ages by LA-ICP-MS

Simultaneous analysis of U–Pb ages and in-situ trace element concen-tration by LA-ICP-MS provides high spatial resolution and has provedto be a reliable technique for extracting zirconU–Pb ages even fromCeno-zoic rocks (e.g. Ballard et al., 2001; Harris et al., 2004; Yuan et al., 2003).

For this study, we used the LA-ICP-MS housed at USTC, and isperformed on the same Elan 6100 DRC ICP-MS instrument used for ele-mental analyses. Before the laser ablation, cathode-ray luminescenceimages (CL images) were obtained for selecting the analytical spots.During the analyses, we used the standard silicate glass NIST (610,612 and 614) to optimize the system, Zircon 91500 as the external stan-dard for U–Pb dating, and NIST 610 glass as the standard for trace ele-ment analysis. Generally, 36-micrometer diameter spots were used,with 24- or 60-micrometer diameters sometimes, depending on thesize of the analyzed zircons. Final isotopic ratios and ages of the zirconswere processed using the CommPbCorr program (Andersen, 2002). Theweighted mean 206Pb/238U ages calculated using the ISOPLOT program(Ludwig, 2001) were used to represent the ages of the rocks.

3.4. Sr–Nd isotopic composition

All Sr–Nd isotopes were isolated at the CAS Key Laboratory of Crust–Mantle Materials and Environments, University of Science and Technol-ogy of China, Hefei (USTC) and the isotopic ratios were measured atTianjin Institute of Geology and Mineral Resources, China GeologicalSurvey. Following sample decomposition, the Sr and the light rare-

Wul

ian-

Mup

ing

Fault

JiaobeiLuxi

Tan

-Lu

Fau

lt Z

on

e

Su-Lu Orogens

Fig. 1. Sketch geological map of the Shandong province showing sample locations. The plutons with abnormally low δ18O values are shown.

354 H.-O. Gu et al. / Lithos 177 (2013) 352–365

earth elements were isolated on quartz columns by conventional-ionexchange chromatography with a 5-ml resin bed of AG 50 W-X12(200–400 mesh). Nd was separated from other rare earth elements onquartz columns using 1.7 ml Teflon powder coated with HDEHP, di(2-ethylhexyl) orthophosphoric acid, as cation exchange medium. Sr andNd were both loaded as phosphate on pre-conditioned Re filaments.Sr and Nd isotopic data were obtained using a Finnigan Triton massspectrometer. Analyses on the standard solutions of NBS 987 and LRIGyielded mean values of 0.710239 ± 0.000003 (2σ) for the 87Sr/86Srratio and 0.512196 ± 0.000003 (2σ) for the 143Nd/144Nd ratio, duringthis study. More details on analytical procedures are given in Chenet al. (2000, 2007).

4. Results

4.1. Whole-rock major and trace element geochemistry

Thewhole rockmajor and trace elemental compositions are listed inElectronic Appendix A. Based on the Sr/Y vs. Y(ppm) relationship (pro-posed by Defant and Drummond (1990) in identifying adakitic rocks)together with the composition of melt from partial melting experi-ments of basalts (usually withMg# b 0.50, Rapp et al., 1999), we subdi-vide the studied plutons into three groups: (i) high Mg adakitic rocks(HMA, usually with Sr/Y N 20, Y(ppm) b 18, Mg# N 0.50); (ii) low Mgadakitic rocks (LMA, usually with Sr/Y N 20, Y(ppm) b 18 andMg# b 0.50) and (iii) normal granitoids (Sr/Y b 20).

Comparable to adakites in modern arcs and those derived fromdelaminated LCC (e.g. Defant and Drummond, 1990; Huang et al.,

2008), the HMA reported in this study show high MgO, Cr and Ni con-tents with Mg# N 0.50. In contrast, the LMA in our study have low con-tents of MgO, Cr and Ni, similar to the compositions of (i) melts frompartial melting experiments of basalts (Rapp and Watson, 1995,1995;Rapp et al., 1991, 1999; Sen and Dunn, 1994), (ii) melts derived fromthickened continental crust (Atherton and Petford, 1993), and (iii) Ar-chean high Sr/Y TTG suites (Condie, 2005; Smithies, 2000). With a fewexceptions, normal granitoids usually have lower Sr contents, Sr/Yratio and higher Y relative to the LMA and HMA (Fig. 5a).

The LMA, HMA and normal granitoids share similarities in somemajor element behavior in Harker diagrams (e.g. Fig. 2). In the diagramof total alkali versus SiO2, normal granitoids clustermainly in the granite,quartz monzonite, monzodiorite and monzonite fields, with a largevariation in SiO2. These plutons show metaluminous to weaklyperaluminous characters (average 0.93, Fig. 3)which are typical for igne-ous sources (Chappell and White, 1992). In contrast, most of the LMAand HMA have more or less higher Al and Mg contents but lower Kthan those of normal granitoids. Notably, the HMA and LMA have higherNa2O/K2O than normal granitoids at a given SiO2, which is also found inclassic adakites (Defant and Drummond, 1990).

In REE patterns, the normal granitoids generally show LREE-enrichednature without obvious negative Eu anomalies and/or concave REE pat-terns (Fig. 4). The HMA and LMA also have LREE-enriched patterns with-out any obvious Eu anomalies. In trace element spider diagrams, all therocks show similar features. They are characterized by enrichment oflarge ion lithophile elements (LILE, e.g. Th. U and Pb) and depletion inhigh field strength elements (HFSE, e.g. Nb, Ta and Ti). Compared to nor-mal granitoids, the HMA and LMA usually have positive Sr-anomalies

Granite

GranodioriteDioriteGDGabbro

QMSyenite

M

MD

4

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16

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50 60 70 80 50 60 70 800.1

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Na 2O

+K2O

HMALMANG

Na 2O

Al 2O

3

TiO

2

Fe 2O

3t

MgO

Ni(p

pm)

SiO2

Sr(p

pm)

SiO2

a b

c d

e f

g h

Fig. 2. The total alkali (Na2O + K2O) versus SiO2 (Irvine and Baragar, 1971; Middlemost, 1985) and Harker diagrams for high-Mg adakitic rocks (HMA), lowMg adakitic rocks (LMA) andnormal granitoids (NG).

355H.-O. Gu et al. / Lithos 177 (2013) 352–365

(Fig. 4). Furthermore, our HMA and LMA samples show low Rb/Ba ratioand are depleted in Rb content, which are considered as typical featuresof lower continental crust (Rudnick and Gao, 2005).

4.2. Whole-rock oxygen isotope

Whole-rock oxygen isotopic data are also listed in Electronic AppendixA. Most of the plutons examined in this study have δ18O values rangingfrom 6 to 10‰, which arewithin the normal values of granitoids. Howev-er, some samples have light oxygen isotopic compositions, with δ18Ovalues as low as 0.9‰. And the samples displaying low δ18O values arefrom plutons located within the Su-Lu orogen belt of Jiaodong (Fig. 1).

4.3. Zircon U–Pb geochronology

High Th/U (mean 1.04), REE patterns typical of magmatic zirconsand magmatic zonings in CL images (Fig. 7) suggest that the zircons

from these plutonsmostly crystallized frommagmas. However, the zir-cons from Luxi, Su-Lu orogen and Jiaobei display some differences bothin petrology and age data.

In Luxi (located to the west of the Tan-Lu fault), the zircons definethree groups of emplacement ages (Fig. 8a–c). These (from north tosouth) are Jinling, Yangtao and Laowa. Zircons from the three granitoidsare generally pale yellow, translucent, euhedral or subhedral. The CL im-ages demonstrate thatmost of the zircon grains are oscillatory zoned. Re-sidual zircon cores are observed in some grains from the Yangtao andLaowa granitoids, but are rare in the Jinling granitoid. Seventeen analyti-cal spots of Laowa zircons yield a weighted mean 206Pb/238U age of134 ± 3 Ma (2 sigma, MSWD = 1.3), representing the formation ageof this pluton, whereas the inherited zircons yield concordant ages rang-ing from 250 to 2500 Ma. The Jinling granitoid yields a formation age of132 ± 4 Ma (206Pb/238U ages, 2 sigma, MSWD = 1.11) based ontwenty-eight analytical spots and no inherited zircons were found. Aweighted mean 206Pb/238U age of 132 ± 4 Ma (2 sigma, MSWD = 1.2)

0.5

1.0

1.5

2.0

2.5

0.5 1.0 1.5 2.0 2.5

3.0

A/N

K

A/CNK

Fig. 3. The A/NK versus A/CNK diagram. A/NK and A/CNK are molar ratios of Al2O3/(Na2O + K2O) andAl2O3/(CaO + Na2O + K2O), respectively. Legends are the same as Fig. 2.

356 H.-O. Gu et al. / Lithos 177 (2013) 352–365

was obtained from eighteen spots in zircons from the Yangtao granitoid,and no concordant inherited ageswere obtained (206Pb/238U ages show arange of 390–3000 Ma).

The zircons from ten granitoid plutons within the Su-Lu orogenicbelt (located to the east of the Tan-Lu fault and to the north of theWulian–Muping fault) (Fig. 8d-m) are mostly idiomorphic withneedle-like shapes (length/width ratios vary from 3:1 to 7:1). Brightrounded rims are not observed, suggesting that the post-magmatichigh temperature hydrothermal alternation is minimal. The age data

RE

E/C

1 C

hond

rite

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hond

rite

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rite

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LMA

NG

1

10

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1000

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1000

LuYbTmDy Ho ErSm Eu Gd TbLa Ce Pr Nd

Fig. 4.Chondrite normalized REE and primitivemantle (McDonough and Sun, 1995; Sun andMc2005, N-MORB values are after Sun and McDonough, 1989. Legends are the same as Fig. 2).

indicate that these widely distributed plutons formed in a short periodbetween 115 Ma and 130 Ma. Some residual zircons yield ages of~220 Ma and ~780 Ma (Fig. 8), which might record the collision be-tween the SCB (South China Block) and the NCC and the Neoproterozoicbasement of the SCB, respectively.

Four plutons from Jiaobei (located to the north of the Su-Lu orogenbut to east the Tan-Lu fault) were dated: Linglong, Guojialing, Guanshuiand Yinpan. The morphology and internal structures of zircons fromthese rocks are similar to those from the Su-Lu orogen belt. The grainsare idiomorphic with obvious magmatic oscillatory zoning, displayinghigh length to width ratios and include many inherited grains. The agedata constrain the timing of formation of the Linglong granite as141 ± 8 Ma (weightedmean of 13 spots, MSWD = 4.6), with inheritedzircon cores displaying ages in the range of 1800–2500 Ma. TheGuojialing granitoid shows an age around130 Ma (131 ± 2 Ma,weight-ed mean of 24, MSWD = 0.7) with old concordant ages of 200 to2100 Ma. The age of the Guanshui granitoid is 153 ± 4 Ma based onthe weightedmean of 16 spots (MSWD = 0.98), with complex old con-cordant ages of 210 to 2000 Ma.Meanwhile, Yinpan granitoid yielded anage of 123 ± 4Ma (weighted mean of 22 spots, MSWD = 2.4).

Collectively, the zirconU–Pb data showEarly Cretaceous ages of 115–135 Ma for most plutons studied here (Table 1 and Fig. 8). Only theGuanshui granitoid displays Late Jurassic ages of 153 ± 4 Ma. Inheritedzircon ages of ~220 Ma and ~780 Mawere found in zircons fromplutonswithin/proximal to the Su-Lu belt, suggesting that recycled crust of theYangtze Block might have contributed to the sources of these plutonsas such ages have not been reported from the basement rocks of theNCC. Notably, the Paleoproterozoic and Neoarchean ages of ~1800 Ma

HMA

Rb Ba Th U Nb Ta La Ce Pb Pr Sr Nd Zr Hf Sm Eu Gd Tb Dy Y Ho Er TmYb Lu

1

10

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1000

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ce E

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ents

/Pri

miti

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antle

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ce E

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ents

/Pri

miti

ve M

antle

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ce E

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ents

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Donough, 1989) normalized trace element patterns. (LCC values are after Rudnick andGao,

0

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Yb)

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Literature data of HMA&LMA from studied areaHMA&LMA from this studyNormal granitoids from this study

Sr/Y

Y(ppm)

0 100 200 300Sr/Y

up to >700

a

b

Fig. 5. Sr/Y versus Y (ppm) (Defant and Drummond, 1990) and (Gd/Yb)N versus Sr/Y (Heet al., 2011; Huang and He, 2010) diagrams for adakitic rocks (literature data are fromYang et al., 2005, 2012a; Zhang et al., 2010).

50 60 70 800.0

0.3

0.6

0.9

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SiO2

0.2 0.4 0.60.1

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1000

Ni(

ppm

)

Mg#

0.2 0.4 0.60.1

1

10

100

1000

Cr(

ppm

)

Mg#

Fields of experimental melts

Fig. 6.Mg# versus SiO2, Cr(ppm) versus Mg# and Ni(ppm) versus Mg# diagrams. The fieldof experimental melts at 1–4 GPa is after Rapp et al. (1999). Legends are the same as Fig. 5.

357H.-O. Gu et al. / Lithos 177 (2013) 352–365

and ~2500 Ma in xenocrystic zircons from Luxi and Jiaobei areas clearlyindicate contribution from the ancient basement of the NCC in themagma generation of these plutons.

4.4. Sr–Nd isotopic composition

Sr–Nd isotopic data for the studied plutons are presented in Table 2,and initial 87Sr/86Sr and 144Nd/143Nd ratios are calculated for the ages ofmagma crystallization (Table 2). The Luxi HMA show initial 87Sr/86Sr ra-tios ranging from 0.705165 to 0.708631, along with the εNd(t) valuesranging from−17.1 to−4.0. Previous studies of the Luxi HMA reporteda broad range of initial 87Sr/86Sr ratios and εNd(t) values (e.g., Yanget al., 2012a). The initial 87Sr/86Sr ratios ranging from 0.709388 to0.710600 and the εNd(t) ranging from −17.5 to−11.6 were obtainedfor the Jiaobei HMA. Inside the Sulu orogenic belt, the initial 87Sr/86Sr ra-tios of the LMA show a range of 0.708050 to 0.710230 and their εNd(t)values range from−20.0 to−14.4,more or less similar to the values re-ported in previous studies. The normal granitoids show initial 87Sr/86Srratios and εNd(t) values of 0.708724 to 0.711982 and−18.7 to−14.4.

5. Discussion

5.1. Petrogenesis of high and low-Mg adakitic rocks in the southeasternmargin of the NCC

5.1.1. Genesis of adakitic rocks in the southeast margin of NCCOne of the most favored models for the genesis of adakites/adakitic

rocks is the partial melting of a subducted oceanic slab. Among the var-ious alternativemodels are the AFC process and partialmelting of lowercrust.

Castillo et al. (1999) suggested that an evolved rock with adakiticcomposition could be generated by the AFC process of evolving basalticmagmas. However, the AFC process is not favored for the petrogenesisof the adakitic rocks investigated in this study based on the followingreasons. There are no mafic plutons of the required size in our studyarea with late Jurassic to early Cretaceous ages. Although the oceanicversus continental source of adakitic rocks remains debated, the highK/Na ratio (mostly N 0.7) and rather low Ce/Pb ratio (mostly b 10) ofthe studied rocks are in contrast to the features of oceanic adakites(e.g. Liu et al., 2010; Xie et al., 2012). Furthermore, these adakiticrocks are located within an intracontinental setting and most of themhave features typical of crustally derived melts. Especially the LMAshare isotopic ratios similar to those of the Dabie LMA, which arewidelyaccepted as the melt products of the LCC (Fig. 9). All the above features

Indicators and Pluton locations: Luxi: a. Jinling b. Laowa c. YangtaoSulu:

d. Dongchen e. Hubu f. Laoshan g. Maoshan h. Qianshigouya i. Rizhao j. Shanyang k. Wulian l. Xuejiadao m. Yaojiazhuang Jiaobei:

n. Guanshui o. Guojialing p. Linglong q. Yinpan

a b c

d e f

g h i

j k l

m

n o

p q

Fig. 7. Representative CL images of zircons from Shandong together with spot ages.

358 H.-O. Gu et al. / Lithos 177 (2013) 352–365

are consistent with the previous conclusion that adakitic rocks inNorth China most likely originated from the LCC (Xiong et al.,2011).

5.1.2. Interaction between adakitic melts and asthenospheric mantleAs demonstrated by experimental studies on interaction between si-

licic melt and peridotite (Rapp and Watson, 1995), partial melts frombasaltic rocks should have low Mg# (usually b0.45), regardless ofwhether the source is from subducted oceanic slab or lower crustalmafic rocks. However, some of the adakitic rocks of the present studyshow higher Mg# than those from experimental melts (Fig. 6a). Sinceour rocks were most likely derived from a continental source, the low-Mg adakitic rocks (Mg# are generally below 0.5) in eastern China arethought to be formed by melting of the thickened LCC. For the high-Mg adakitic rocks (Mg# > 0.5), the most likely genetic mechanism isthe reaction of adakitic melts (derived from the delaminated LCC) andhot asthenospheric mantle (Xu et al., 2003a,b, 2004, 2006a,b, 2009;Yang et al., 2011; Zhang et al., 2010; Zi et al., 2007). We employ the Crvs.Mg# andNi vs.Mg# relation to identify the addition ofmantlemate-rials during reactions between the delaminated lower continental crustand asthenospheric mantle, which clearly distinguish the high-Mgadakitic rocks and low-Mg adakitic rocks studied here (Fig. 6b and c).

Ni and Cr are much more compatible in mantle materials than in felsicmagmas and, hence, even the addition of minor mantle materials willsignificantly raise the Cr, Ni and Mg# with simultaneous decrease inSiO2. In addition, mantle xenoliths from some high-Mg adakitic rocksmay provide some direct evidence of reactions between adakitic meltsand mantle peridotites (Xu et al., 2008). From the Sr–Nd isotope dia-gram (Fig. 9), the HMA also show a trend of mixing of the underlyingmantle and the crust-derived magmas, which decreases the Sr ratioand increases the Nd ratio simultaneously.

Based on the above features, we suggest that the low-Mg adakiticrocks studied here originated from a thickened lower continentalcrust, whereas the high-Mg adakitic rocks were generated by meltingof delaminated lower continental crust and its reaction with the under-lying mantle peridotites.

5.2. Low δ18O Mesozoic granitoids within the Su-Lu orogen belt

Various examples of low δ18ΟMesozoic granitoids have beenwidelyobserved within the Dabie orogenic belt (e.g. Xu et al., 2005; Zhao andZheng, 2009; Zhao et al., 2004, 2007). However, only a few examplesof low δ18Ο Mesozoic granitoids have been reported so far from theSu-Lu orogen (Huang et al., 2006; Zhang et al., 2010). Based on in-situ

Mean=130.6±2.2 MaMSWD=0.7

Mean=132.2±3.9 MaMSWD=1.11

Mean=133.6±3.4 MaMSWD=1.3

Mean=131.8±3.7 MaMSWD=1.2

Mean=125.1±3.1 MaMSWD=1.3

Mean=125.5±2.2 MaMSWD=1.6

Mean=122.4±2.1 MaMSWD=2.7

Mean=124.0±3.6 MaMSWD=0.66

Mean=128.7±4.2 MaMSWD=1.5

Mean=123.2±4.7 MaMSWD=2.0

Mean=127.1±2.6 MaMSWD=1.2

Mean=124.3±5.3 MaMSWD=1.3

Mean=119.0±1.7 MaMSWD=1.3

MSWD=0.69Mean=118±3.9 Ma Mean=152.9±4.3 Ma

MSWD=0.98

Mean=141.0±8.0 MaMSWD=4.6

Mean=123.3±3.6 MaMSWD=2.4

Sample locations: Luxi: a, b, c Sulu: d, e, f , g, h, i, j, k, l, m Jiaobei: n, o, p, q

a b c

d e f

hg i

kj l

m n o

p q

Fig. 8. Concordia diagrams of zircons along with REE patterns.

359H.-O. Gu et al. / Lithos 177 (2013) 352–365

Table 1Zircon U–Pb ages of the Mesozoic intrusions in Shandong Province measured by LA-ICP-MS.

No. Sample No. Region Pluton/location Rock type Age(Ma) MSWD

1 07-HT-01 Luxi Jinling HMA 132.2 ± 3.9 1.112 07-LW-06 Luxi Tietonggou (Laowa) HMA 133.6 ± 3.4 1.303 07-YT-02 Luxi Yangtao HMA 131.8 ± 3.7 1.204 08-GJL-02 Jiaobei Guojialing HMA 130.6 ± 2.2 0.705 08-LL-01 Jiaobei Linglong HMA 141.0 ± 8.0 4.606 08-YP-01 Jiaobei Yinpan HMA 123.3 ± 3.6 2.407 07-MS-03 Su-Lu Rizhao (Miaoshan) LMA 124.0 ± 3.6 0.668 08-GS-03 Jiaobei Guanshui LMA 152.9 ± 4.3 0.989 08-SY-05 Su-Lu Wulian (Shanyang) LMA 127.1 ± 2.6 1.2010 07-RZ-01 Su-Lu Rizhao LMA 123.2 ± 4.7 2.0011 08-WL-01 Su-Lu Wulian LMA 124.3 ± 5.3 1.3012 08-XJD-02 Su-Lu Xuejiadao LMA 119.0 ± 1.7 1.3013 07-QSGY-03 Su-Lu Qianshigouya NG 128.7 ± 4.2 1.5014 08-HB-01 Su-Lu Wulian (Hubu) NG 125.5 ± 2.2 1.6015 08-DC-01 Su-Lu Laoshan (Dongchen) NG 125.1 ± 3.1 1.3016 08-YJZ-03 Su-Lu Yaojiazhang NG 118.0 ± 3.9 0.6917 08-LS-01 Su-Lu Laoshan NG 122.4 ± 2.1 2.70

0.700 0.705 0.710 0.715 0.720

-40

-30

-20

-10

0

10

εNd (

t)

ISr

Lower Continental Crust

Young Upper Continental Crust

KonglingM

antle array

HMA from Luxi

HMA and LMAfrom Jiaobei

LMA from Su-Lu and Dabie

HMA from Dabie

Fangcheng basalt

Melt/rock interaction?

Fig. 9. εNd(t) vs. initial 87Sr/86Sr plots for a variety of high Mg adakitic rocks, low Mgadakitic rocks and normal granitoids. Data source: HMA from Luxi (Yang et al., 2012a),LMA and HMA from Jiaobei (Zhang et al., 2010), HMA from Dabie (Huang et al., 2008),LMA fromDabie and Sulu (Wang et al., 2007; Xu et al., 2007; Yang et al., 2005), lower con-tinental crust of East China and young upper continental crust (Jahn et al., 1999).

360 H.-O. Gu et al. / Lithos 177 (2013) 352–365

zircon analyses from the granitic gneiss in the Jiaodong Peninsula, it hasbeen concluded that the protoliths of these granitoids are also charac-terized by very low δ18O values (Tang et al., 2006; Tang et al., 2008).

Our results show that low δ18O granitoids are distributed in a ratherbroad area across the Su-Lu orogenic belt (Fig. 1). One of themost plau-sible ways to generate these low δ18O granitoids is from low δ18Omagmas (Huang et al., 2006; Zhang et al., 2010), and therefore, thesegranitoids represent the occurrence of low δ18Ο Mesozoic granitoidswithin the Su-Lu belt. Furthermore, some of these low δ18O granitoidshave inherited zircon ages falling in the ranges of Neoproterozoic tolate Triassic (Fig. 7d ~ m), suggesting that the subducted YangtzeBlock may have significantly contributed in generating the low-δ18O-magmas. This is also consistentwith previous suggestions on the forma-tion of the Mesozoic magmatic rocks by remelting of subducted conti-nental lithosphere of the SCB (Zhao and Zheng, 2009).

5.3. Geochronological constrains on the low-Mg adakitic rocks from theDabie and the Su-Lu orogens

The Dabie and Su-Lu orogens are thought to have been connectedduring the middle-Triassic subduction of the SCB, and were offset byabout 500 km through the strike-slip movement of the Tan-Lu fault inthe Mesozoic (Wang, 2006; Yang, 2006; Zhu et al., 2004, 2005). As thetime series of magmatic rocks can be used to trace their tectonic

Table 2Sr–Nd isotopic composition of the Mesozoic intrusions in Shandong Province (Initial Sr–Nd iso

Sample No. Rock Type 87Sr/86Sr Error 143Nd/14

07-HT-01 HMA 0.705547 0.000004 0.51237707-LW-01 HMA 0.706696 0.000004 0.51228607-LW-04 HMA 0.707367 0.000004 0.51229607-ZZYN-03 HMA 0.709934 0.000003 0.51166908-YP-01B HMA 0.757702 0.000004 0.51185908-HY2-01 HMA 0.710435 0.000004 0.51181508-GJL-02 HMA 0.711329 0.000003 0.51196508-LL-02 HMA 0.711149 0.000004 0.51176808-QBS-03 LMA 0.708602 0.000002 0.51180607-ZK-02 LMA 0.709046 0.000004 0.51163807-RZ-02 LMA 0.711311 0.000004 0.51153407-QS-02 LMA 0.709285 0.000002 0.51167108-ZZ-02 LMA 0.710489 0.000004 0.51160508-XJD-01 LMA 0.711357 0.000003 0.51168408-GS-01 LMA 0.712171 0.000004 0.51157908-SB-01B LMA 0.709487 0.000004 0.51168408-HB-04 NG 0.749025 0.000005 0.51169208-YJZ-03 NG 0.720797 0.000003 0.51180608-HB-01 NG 0.735459 0.000005 0.511738

environments (Zhang et al., 2003b, 2008), a comparison of the geochro-nology of low-Mg adakitic rocks from the Dabie and Su-Lu orogens canoffer information on the evolutionary history of these two areas.

There is nomarked difference in the inherited ages from zircons be-tween low-Mg adakitic rocks from the Su-Lu orogen and those from theDabie orogen. The Neoproterozoic (573–842 Ma, 3 samples), Triassic(210–260 Ma, 3 samples), and Paleo-Mesoproterozoic (1.3–2.0Ga, 2samples) ages obtained from the Su-Lu low-Mg adakitic rocks, bothconcordant and discordant, can also be found in the low Mg adakiticrocks from Dabie (He et al., 2011; Wang et al., 2007). This is consistentwith known zircon U–Pb ages for the protoliths of theUHPmetaigneousrocks in the Dabie-Sulu orogenic belt (Zhao and Zheng, 2009), indicat-ing that the subducted SCBmade significant contributions to the forma-tion of the Su-Lu low-Mg adakitic rocks. The data therefore suggest auniquemagma source for the lowMg adakitic rocks from the two areas.

Secondly,most of the low-Mg adakitic rocks from the Su-Lu area haveformation ages of 120 to 130 Ma (with a mean age of 123 Ma), whereas

topic composition was calculated at the formation age of the plutons).

4Nd Error (87Sr/86Sr)i (143Nd/144Nd)i εNd(t)

0.000001 0.705165 0.512266 −4.00.000005 0.706075 0.512176 −5.60.000002 0.706746 0.512186 −5.40.000003 0.708631 0.511599 −17.10.000003 0.710002 0.511772 −13.90.000002 0.710377 0.511740 −14.60.000002 0.710600 0.511877 −11.60.000004 0.710923 0.511695 −14.80.000003 0.708055 0.511739 −14.40.000003 0.708484 0.511555 −18.00.000005 0.708953 0.511453 −20.00.000002 0.709223 0.511589 −17.30.000003 0.710162 0.511534 −18.40.000003 0.710230 0.511603 −17.20.000004 0.711982 0.511482 −18.70.000003 0.708161 0.511613 −16.90.000005 0.708724 0.511615 −16.80.000006 0.709142 0.511749 −14.50.000002 0.710200 0.511660 −15.9

361H.-O. Gu et al. / Lithos 177 (2013) 352–365

those from the Dabie area have ages generally N130 Ma (129–142 Ma,with amean of 133 Ma,Wang et al., 2007). Notably, there is a systematicdifference in the formation ages between lowMg adakitic rocks from thetwo areas, indicating a lateral extension of the Su-Lu orogen as comparedto the Dabie orogen. Among the adakitic rocks in the Dabie orogen, theLMA yield greater ages compared to the HMA. Our data show an inversesequence (i.e. the ages of HMA are greater than those of the LMA), butwith the same spatial distribution (from the west to the east). This sys-tematic temporal and spatial distribution suggests a west-eastwardforce that generated the magmatism. As the main heat source formagmatism is asthenospheric upwelling, our data suggest that the up-welling of the asthenosphere underlying Eastern China in the Mesozoiccouldmigrate from thewest to the east and thismight also have contrib-uted to the lithospheric thinning process. On the other hand, the agedifference between low-Mg adakitic rocks from the two areas also com-pares well with the age difference in magmatism between the Lu-ZongBasin and the Jiaolai Basin. The main magmatic events in the Lu-Zongbasin, located in the northernmargin of the Yangtze Block, occurred dur-ing 124 to 136 Ma (Wang et al., 2006a; Zhai et al., 1996). In contrast, themain volcanic event in the Jiaolai Basin, located within the NCC, was at~110 Ma (Han et al., 1993). This systematic differencemay reflect differ-ent post-collision extensional histories in the Dabie and Su-Lu orogensafter their separation by the Tan-Lu fault.

5.4. Geodynamics of initiation of lithosphere thinning in East China: role ofthe Tan-Lu fault

As shown in Fig. 10, the high-Mg adakitic rocks are mostly distribut-ed parallel to the Tan-Lu fault whereas most of the low-Mg adakiticrocks occur inside the orogenic belts (both in the Su-Lu and the Dabiebelts). Considering their spatial distribution, the high-Mg adakiticrocks near the northern part of the Tan-Lu fault were emplaced to thewest of the fault whereas those near the southern part are mostly dis-tributed to the east and are proximal to the fault. In terms of temporal

Fig. 10. Sketchmap showing the spatial and temporal correlations between the adakitic rocks a

distribution, the low-Mg adakitic rocks in the Dabie orogen belt (143–129 Ma), high-Mg adakitic rocks along the Tan-Lu fault (134–128 Ma)and low-Mg adakitic rocks in the Su-Lu orogen belt (127–120 Ma) de-fine a younging sequence (Fig. 10).

The Jiaolai and Luzong basins are more or less connected with theMesozoic strike-slip direction of the Tan-Lu fault. The Tan-Lu fault con-trols at least one border of the two basins, i.e., the western border of theLu-Zong basin and thewestern and southern borders of the Jiaolai basinalong with the Wulian–Muping fault. The Tan-Lu fault has cut throughthe lithosphere and generated extensive ore mineralization in the areaincluding several gold deposits some of which clearly display mantlecontribution (Guo et al., 2013; Han et al., 1993; Mao et al., 2011;Wang et al., 2006a).

The features related to the spatial and temporal distribution alongwith the correlations between the Tan-Lu fault and the two basinsimply connections between the late-Jurassic to early-Cretaceousadakitic magmatism and the strike-slip of the Tan-Lu fault. Below wediscuss the possibility that the large-scale strike-slip of the Tan-Lufault played an important role in the initiation of lithosphere thinningin the southeast margin of the NCC (Fig. 11).

The strike-slip movement along the Tan-Lu fault was initiated fromlate Jurassic (N140 Ma) (Wang, 2006; Zhang et al., 2003b; Zhu et al.,2010, 2012). The deep-seated large-scale strike-slip movement led tosmall scale delamination of the underlying lower crust. High Mgadakitic melts might have been generated in this timescale or later byinteractions between the delaminated segments' melts (which isadakitic) and the mantle, increasing the Mg# of the melts (from 0.28to at least 0.67, estimated from our studied samples). The Tan-Lu faultrecords an extensional history until the early Cretaceous (Zhu et al.,2010, 2012). The high-Mg adakitic melts generated were emplacedinto the upper crust during this extension at 135–128 Ma. At the sametime, the deep-seated movement of this major fault might have alsoweakened the lithosphere beneath the Su-Lu orogenic belt. During130–125 Ma, low Mg adakitic magmas were generated by direct

nd the TLF (Some age data are from Huang et al., 2008; Wang et al., 2007; Xu et al., 2004).

362 H.-O. Gu et al. / Lithos 177 (2013) 352–365

melting of the thickened lower continental crust beneath the Su-Lu oro-genic belt as a result of heating by asthenospheric upwelling. This wasfollowed by large-scale lithosphere thinning, resulting in the wide-spread emplacement of granitic rocks in Eastern China.

6. Conclusion

Bothhigh and low-Mg adakitic rocks aswell as normal granitoids arewidely distributed along or adjacent to the Tan-Lu fault in East China.

Fig. 11. Cartoons showing the geodynamic processes of lithosphere thinning in East China. The lfor initiating the lithospheric thinning of the southeast margin of the NCC.

The high-Mg adakitic rocks were probably generated by reactions be-tween delaminated lower crust and the mantle, whereas the low-Mgadakitic rocks are probable products of melting from thickened lowercrust. The normal granitoids might have originated from middle tolower crust.

The high-Mgadakitic rocks are distributed along a belt parallel to theTan-Lu fault, mostly recognized in the western domain of the fault. Incontrast, the low-Mg adakitic rocks are located inside the orogenicbelts. Zircon U–Pb ages constrain the formation time of the high-Mg

arge-scale strike slipmovement along the Tan-Lu fault might have acted as themechanism

363H.-O. Gu et al. / Lithos 177 (2013) 352–365

adakitic rocks as around 130 Ma, with the low-Mg adakitic rocksformed slightly later (127–120 Ma). Our results reveal that the Tan-Lufault played an important role in initiating the Mesozoic lithosphericthinning process of the southeast margin of the North China Craton.

Within the Su-Lu orogen, some of the LMA show low whole-rockδ18O values suggesting the contribution from remelted subducted litho-sphere of the SCB.

Supplementary data to this article can be found online at http://dx.doi.org/10.1016/j.lithos.2013.07.011.

Acknowledgments

We thank Lithos Editor Prof. Nelson Eby and two anonymous ref-erees for constructive reviews and useful suggestions. Profs. ShuguangLi and Hongfu Zhang are thanked for the field work. We also appreciatethe constructive suggestions from Prof. Shuguang Li and Dr. Sheng-AoLiu at the early stage of this paper. This study was financially supportedby the Chinese grants NSFC 90814008 and 41172067, and the HundredTalent Program of the CAS for YL. Xiao. This is also a contribution to the1000 Talent Award to M. Santosh from the Chinese Government.

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