Timing, mantle source and origin of mafic dykes within the gravity anomaly belt of the Taihang-Da Hinggan gravity lineament, central North China Craton

Accepted Manuscript Title: Timing, mantle source and origin of mafic dykes within the gravity anomaly belt of the Taihang-Da Hinggan gravity lineament, central North China Craton Authors: Shen Liu, Caixia Feng, Guangying Feng, Mengjing Xu, Ian M. Coulson, Xiaolei Guo, Zhuang Guo, Hao Peng, Qiang Feng PII: DOI: Reference:

S0264-3707(16)30242-3 http://dx.doi.org/doi:10.1016/j.jog.2017.05.006 GEOD 1491

To appear in:

Journal of Geodynamics

Received date: Revised date: Accepted date:

7-12-2016 24-5-2017 25-5-2017

Please cite this article as: Liu, Shen, Feng, Caixia, Feng, Guangying, Xu, Mengjing, Coulson, Ian M., Guo, Xiaolei, Guo, Zhuang, Peng, Hao, Feng, Qiang, Timing, mantle source and origin of mafic dykes within the gravity anomaly belt of the TaihangDa Hinggan gravity lineament, central North China Craton.Journal of Geodynamics http://dx.doi.org/10.1016/j.jog.2017.05.006 This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain.

Timing, mantle source and origin of mafic dykes within the gravity anomaly belt of the Taihang-Da Hinggan gravity lineament, central North China Craton

Shen Liu1, Caixia Feng1, Guangying Feng2, Mengjing Xu1, Ian M. Coulson3 Xiaolei Guo1,Zhuang Guo1, Hao Peng1, Qiang Feng1

1. State Key Laboratory of Continental Dynamics and Department of Geology, Northwest University, 229 Taibai Road, Xi'an 710069, China 2. Institute of Geology, Chinese Academy of Geological Sciences, 26 Baiwanzhuang Street, Beijing 100037, China 3. Solid Earth Studies Laboratory, Department of Geology, University of Regina, Regina, Saskatchewan S4S 0A2, Canada

Highlights 

Late Mesozoic mafic dykes in the Taihang-Da Hinggan Mountains, central North China Craton were dated at 122-132 Mas. > The dykes were derived from enriched lithospheric mantle source. > The origin of the dykes is related to the foundered lower crust, and the dykes were derived from partial melting of hybrid mantle source.

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Abstract Six mafic dyke swarms crop out in Hebei Province within the Taihang-Da Hinggan gravity lineament magmatic belt, China, and were sampled. Here, we present new zircon laser ablation-inductively coupled plasma-mass spectrometry U-Pb age, whole rock geochemical, and Sr-Nd-Pb-Hf isotopic data for the six areas where these mafic dykes occur. The mafic (dolerite) dykes formed between 131.6 ± 1.6 and 121.6 ± 1.1 Ma, and are enriched in the light rare earth elements (LREE), some of the large ion lithophile elements (LILE; e.g., Rb, Ba, and Sr) and Pb, and are depleted in Th, U, Nb and Ta; some samples are also depleted in Eu. The dykes have high initial 87Sr/86Sr ratios (0.7055-0.7057), negative Nd (t) values (-12.5 to -11.9), relatively constant Pb isotopic ratios ((206Pb/204Pb)i = 16.45-16.51, (207Pb/204Pb)i = 15.44-15.51, (208Pb/204Pb)i = 36.49-36.53), negative Hf (t) values (-18.2 to -15.1), and old Nd (TNdDM2; 2.17-2.47 Ga) and Hf (THfDM2; 2.28-2.33 Ga) model ages. These geochronological, geochemical, and isotopic data indicate that the dykes were derived from magmas generated by low to moderate degree partial melting (1.0 %-10 %) of an EM1-like garnet lherzolite mantle source; these magmas fractionated olivine, clinopyroxene, and hornblende prior to emplacement, and assimilated minimal amounts of crustal material. Several possible models have previously been proposed to explain the origin of Mesozoic magmatism in this region. However, here we propose a foundering model for these studied mafic dykes, involving the foundering of eclogite from

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thickened lower crust due to the collision between the Siberian Craton and the North China Craon.

Key words: Dolerite, Cretaceous, Taihang-Da Hinggan gravity lineament, Origin, Foundering

1. Introduction The tectonic-magmatic Taihang-Da Hinggan gravity lineament forms the central zone of Mesozoic magmatic activity in eastern China and is defined by a NNE-SSW trending zone of variations in crustal thickness and high gravity gradients (Cai et al., 2004). The compositionally variable and voluminous Mesozoic intrusive rocks in this region (35 °N to 50 °N and 113°E to 125 °E) generally crop out in the southern and northern Taihang areas, and the central to southern Da Hinggan regions (Cai et al., 2004). This magmatism records the geological and dynamic evolution of this area (Niu et al., 1994; Deng, 1996, 2000; Liu and Shi, 1998; Xu et al., 1999; Cai et al., 2003, 2004, 2006; Chen and Zhai, 2003; Chen et al., 2003, 2005, 2006, 2007; Qin, 2005; Shen et al., 2015). However, mafic-ultramafic rocks have only rarely been reported from this region. The mantle source and origin of Mesozoic igneous rocks thus remain debated (Li and Yu, 1993; Yu, 1995; Shao et al., 1999a; Qian et al., 2002; Cai et al., 2003, 2004; Zhang et al., 2004). The magmatic Taihang-Da Hinggan gravity lineament contains voluminous

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mafic dykes, monzonites, A-type granites, high-K I-type volcanic rocks, bimodal volcanic rocks, and alkaline igneous rocks, as well as extensional basins (Sun et al., 1997), and detachment fault zones (Zhang et al., 2002), all of which suggest that this area underwent significant extension during the Mesozoic. However, the exact timing of this extension, the dynamic processes that caused this stretching event, and the source and origin of the contemporaneous magmatism have not yet been identified. Mafic dykes can form as a result of extension of the continental lithosphere (Hall, 1982; Zhao and McCulloch, 1993), meaning that these units may provide valuable information on the evolution of the lithosphere, including extensional tectonics, mantle composition(s), and the temporal and spatial evolution of that part of the Earth’s lithosphere. In addition, investigating these dykes can provide insights into the origin of other magmatic units within the Taihang-Da Hinggan gravity lineament. Furthermore, Mesozoic mafic dykes are widespread throughout the gravity lineament, and more than 200 mafic rock units (e.g., Laiyuan, Luxian, Quyang, Lingshou, Qixian, Weichang, Fengning, Chicheng, Huailai, and Yixian) have been identified. These units are dominantly dolerite and lamprophyre in composition, although a minor proportion of porphyritic dolerite dykes are also present, and the vast majority of these rocks are present as NW-SE, NE-SW, and E-W trending dyke swarms. Here, we report new representative zircon U-Pb ages, and geochemical and Sr-Nd-Pb-Hf isotopic data for Mesozoic mafic dykes studied from the Weichang, Fengning,

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and Chicheng, Huailai, and Yixian areas of Hebei Province, which falls within the magmatic Taihang-Da Hinggan gravity lineament. These data provide insights into the timing, mantle source, and the origin of the investigated dykes, enable an assessment of the geodynamic processes that caused this magmatism, and provide evidence of the tectonic setting of the magmatism within the magmatic Taihang-Da Hinggan gravity lineament.

2. Geological and tectonic setting The North China Craton (NCC) is one of the oldest continental nuclei worldwide (Jahn et al., 1987; Liu et al., 1992) and is divided into the Eastern, Western, and Central Blocks (Zhao et al., 2001). At present, one of the striking features of the NCC is the gravity anomalies within the NNE-trending Taihang-Da Hinggan gravity lineament of the Central Block. These anomalies are located between the NCC and the Erdos Plateau (Zhang et al., 2002), span both the NCC and the Xingmeng Orogenic belt, are connected to the Yinshan-Yanshanian Belt to the north, and are linked with the Qinling-Dabie Orogenic Belt to the south (Fig. 1). The gravity anomalies within the Taihang-Da Hinggan gravity lineament are also proximal to the Pacific tectonic belt. This means that the study area provides key information on the tectonic evolution of this complex region. The Taihang-Da Hinggan gravity lineament is located in an ancient band of weak rock beneath the NCC, as well the forward position of the subducted paleo-Pacific Plate. In addition, the Taihang-Da

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Hinggan gravity lineament intrudes Paleoproterozoic cryptic basement, during orogenesis, and is surrounded by a significant volume of exposed basement in the central Blocks (Fig. 1). The Mesozoic intrusions within the south Taihang region are generally located in the Hanxing area of Hebei Province, the Ping shun area of Shanxi Province, and the Anyang-Linxian area of Henan province. This magmatism produced a number of major plutons, including the Fusan, Guzhen, Kuangshan, Hongshan, Xi’anli, Dongye, and Huanglongnao-Tashan intrusions that were generally emplaced into Mid Ordovician units and dominantly have gabbro-diorite, diorite-monzonite, and syenite compositions (Cai et al., 2004). In contrast, Mesozoic intrusions in the north Taihang region are generally located in the Fuping-Laiyuan and southeastern Yanshan areas, and the majority are of bimodal series. These plutonic rocks include the Mapping, Chiwawu, Laiyuan, Fangshan, Badaling, Dahaituo, and Wulingshan intrusions, which are dominated by hornblende bearing gabbrodiorite, granodiorite monzonitic granite, and quartz-monzonite - quartz-orthoclase granite - alkaline granite phases (Cai et al., 2004). Other Mesozoic intrusions in this area crop out in the Huanggang, Chaoyanggou, Baiyinruo, Haobugao, Haisuba, Wulanba, Baize, and Nianzishan areas and are dominated by diorite granodiorite, monzonitic granite, quartz monzonite, quartz-orthoclase granite, and alkaline granite compositions (Cai et al., 2004). Three phases of magmatic activity have been recognized in this area (Hebei Bureau of Geology and

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Mineral Resources, 1989; Inner Mongolia Autonomous Region, 1991; Beijing Bureau of Geology and Mineral Resources, 1991; Xu et al., 1996, 1999; Cai et al., 2003). The early magmatic activity occurred between the Early and Mid Jurassic, forming mafic and intermediate rocks. The middle period of magmatic activity occurred during the Late Jurassic, represents the main phase of magma activity within the tectonic-magmatic Taihang-Da Hinggan gravity lineament, and formed intermediate-felsic units (e.g., diorite, monzonite, granite, and syenite units). The third period of magmatism occurred during the Early Cretaceous and generated felsic and alkaline rocks (Cai et al., 2003; Chen and Zhai, 2003; Chen et al., 2003, 2005, 2006, 2007; Peng et al., 2004). The mafic dykes studied here generally have dolerite and lamprophyre compositions, primarily as the study areas did not contain any porphyritic dolerites.

3. Petrography and sampling Mafic dykes are widespread in the five representative areas (i.e., the Weichang, Fengning, Chicheng, Huailai, and Yixian regions) that form the focus of this study, within Hebei Province, northern Taihang gravity lineament (Fig. 2). The study areas contain granite, monzonite, gabbro, and gneissic country rocks, all of which are intruded by mafic dykes, although the majority of the dykes are hosted by granite and Archean-Proterozoic (Qianxi, Fuping, Jixian and Changcheng groups) units (Fig. 2). Individual mafic dykes studied

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are vertical, strike NE-SW, NW-SW, and E-W (Fig. 2), are between 20 m and 60 m wide, have lengths of 8.0-50 km (Fig. 2), and have typical dolerite textures. The mafic dykes studied within the Weichang area were emplaced into monzonites and granites, are vertical, strike between E-W and NW-SE, and have widths of 20-50 m and lengths of 6.0-50 km (Fig. 2). They contain 30 %-35 % of combined clinopyroxene, plagioclase, and minor biotite microphenocrysts (0.5-1.3 mm), within a groundmass (~60 %-70 %) of pyroxene, plagioclase, magnetite, and chlorite. The mafic dykes studied within the Fengning and Chicheng areas were generally emplaced into granitic units, are vertical, strike E-W, NE-SW, and NW-SE, and are 10-60 m wide and 5.0-50 km long (Fig. 2). They contain 30 %-36 % of combined clinopyroxene, alkali feldspar, plagioclase, and minor biotite microphenocrysts (0.5-1.2 mm), within a groundmass (~65 %-70 %) of pyroxene, alkali feldspar, plagioclase, and magnetite. Mafic dykes studied from the Huailai area were emplaced into granitic country rocks, are vertical, strike E-W, NE-SW, and NW-SE, and have widths of 8.0-50 m and lengths of 5.0-40 km (Fig. 2). They contain 30 %-35 % of combined clinopyroxene, alkali feldspar, plagioclase, and minor biotite microphenocrysts (0.5-1.3 mm) in a groundmass (~60 %-65 %) of pyroxene, alkali feldspar, plagioclase, and magnetite. Mafic dykes studied within the Yixian were emplaced into monzonite and

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granite units, are vertical, strike E-W and NW-SE, and are 10-60 m wide and 5.0-40 km long (Fig. 2). They contain 30 %-37 % microphenocrysts (0.5-1.2 mm) of clinopyroxene, plagioclase, and minor biotite within a groundmass (~65 %-75 %) of pyroxene, plagioclase, magnetite, and chlorite.

4. Analytical methods Zircon grains from six of the investigated dyke samples from the northern Taihang gravity lineament of Hebei Province were separated using conventional heavy liquid and magnetic techniques. Representative zircons were then handpicked under a binocular microscope before being mounted in an epoxy resin disc, polished, and coated with gold prior to analysis. These zircon grains were imaged using transmitted and reflected light microscopy, and cathodoluminescence (CL) methods to identify external and internal structures. The CL imaging and U-Pb geochronology analyses were undertaken at the State Key Laboratory of Continental Dynamics, Northwest University. The analytical procedures used are described in detail in Harris et al. (2004) and Campbell et al. (2006), and we used a spot diameter of 29 m. U-Th-Pb ratios and absolute abundances were determined by reference to multiple measurements of a standard TEMORA zircon and a NIST 610 glass standard. In situ, zircon Hf isotopic analyses were undertaken using a multi-collector-inductively coupled plasma-mass spectrometer equipped with a

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Geolas-193 laser at the Key Laboratory of Continental Dynamics, Northwest University. These analyses used a laser repetition rate of 10 Hz at 100 mJ and a beam diameter of either 32 or 63 m. The isobaric interference of 176Lu on 176Hf

was corrected by measuring the intensity of the interference-free 175Lu

isotope and using a recommended 176Lu/175Lu ratio of 0.02655 (Machado and Simonetti, 2001). A 176Yb/172Yb value of 0.5887 (Chu et al., 2002) and mean Yb values obtained during Hf analysis were used to correct for the interference of 176Yb on 176Hf (Iizuka and Hirata, 2005). Details of the analytical and data correction procedures are given in Wu et al. (2006). Our analyses included measurements of standard 91500 and FM0411 zircons, yielding mean 176Hf/177Hf ratios of 0.282313 ± 36 (2 standard deviations (SD), n = 35) and 0.282996 ± 31 (2 SD, n = 9), respectively, which agree with the reported 176Hf/177Hf

composition of the 91500 zircon (0.282306 ± 8, 2 SD, n = 30) by

solution analysis (Wood head et al., 2004) and 0.282983 ± 17 (2 SD, n = 9) for the FM0411 zircon by in situ analysis methods (Wu et al., 2006). The whole-rock and Sr-Nd-Pb isotopic geochemistry of 26 samples studied was determined during this investigation. Prior to analysis, these samples were trimmed to remove altered surfaces before cleaning with deionized water, crushing, and powdering in an agate mill. Major element compositions were determined using an analytical Axioms-advance X-ray fluorescence spectrometer at the State Key Laboratory of Ore Deposit Geochemistry (SKLODG), Institute of Geochemistry, Chinese

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Academy of Sciences, Guiyang, China, using fused lithium tetra borate glass pellets. This analysis has an analytical precision better than 5 %. Trace element compositions were determined by ICP-MS and a Perkin-Elmer ELAN DRC-e instrument at the SKLODG. Prior to analysis, powdered samples (50 mg) were dissolved in high-pressure Teflon bombs using a HF + HNO3 attack for 48 h at ~190 °C (Qi et al., 2000). Signal drift during analysis was monitored using Rh as an internal standard, and GBPG-1, OU-6, GSR-1, and GSR-3 standards were used for analytical quality control, indicating an analytical precision that is generally better than 5 % for trace elements. The Rb-Sr and Sm-Nd isotopic analyses began with the spiking of sample powders with mixed isotope tracers, before dissolution in Teflon capsules using a HF + HNO3 acid attack and separation by conventional cation exchange techniques. Isotopic measurements were undertaken using thermal ionization mass spectrometry at the Isotopic Geochemistry Laboratory of the Yichang Institute of Geology and Minerals Resources, Yichang, China. This analysis yielded procedural blanks of < 200 pg for Sm and Nd, and < 500 pg for Rb and Sr. Mass fractionation corrections for Sr and Nd isotopic ratios were based on 86Sr/88Sr = 0.1194 and 146Nd/144Nd = 0.7219, respectively. Analysis of the NBS987 standard yielded a mean 87Sr/86Sr value of 0.710246 ± 16 (2), and analysis the La Jolla standard yielded a mean 143Nd/144Nd value of 0.511863 ± 8 (2). Prior to Pb isotopic analysis, Pb was separated and purified by conventional cation-exchange techniques (AG1 × 8, 200-400 resin) using

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diluted HBr as an eluent. Analysis of the NBS981 standard yielded a mean 204Pb/206Pb

value of 0.0896 ± 15, a mean 207Pb/206Pb value of 0.9145 ± 8, and

a mean 208Pb/206Pb value of 2.162 ± 2.

5. Results 5.1. Zircon U-Pb ages Zircon is relatively abundant in the dolerite samples, and the majority of zircon grains show oscillatory or planar zoning in CL images, indicating a magmatic origin. None of the studied zircons contain inherited cores and they all have relatively high Th/U ratios (0.37-1.65), again indicating a magmatic origin. Two mafic dykes (WC1 and WC8) from the Weichang area have similar weighted mean 206Pb/238U zircon ages of 131.5  1.2 (n = 11) and 131.6  1.6 Ma (n = 12; Table 1; Fig. 3a, b). One sample (FL2) from a mafic dyke in the Fengning area yielded an age of 127.8  1.0 Ma (n = 10; Table 1; Fig. 3c). Zircon from mafic sample CC1 from the Chicheng area yielded an age of 128.1  1.2 Ma (n = 11; Table 1; Fig. 3d), and zircon from mafic sample HL1 within the Huailai area yielded an age of 121.9  1.4 Ma (n = 11; Table 1; Fig. 3e). Meanwhile, zircon from mafic sample YX3 from the Yixian area yielded an age of 121.6  1.1 Ma (n = 12; Table 1; Fig. 3f).

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5.2. Whole-rock geochemistry The whole-rock compositions of the studied dolerites are given in Table 2-1 and 2-2. These mafic dykes are characterized by slight variations in SiO2 (50.12-51.88 wt. %), Na2O (2.84-3.46 wt. %), Al2O3 (15.48-16.52 wt. %), TiO2 (0.95-1.32 wt. %), and MnO (0.12-0.18 wt. %), but have more variable concentrations of K2O (2.63-3.66 wt. %), Fe2O3 (7.02-9.65 wt. %), MgO (5.08-6.64 wt. %), CaO (6.86-7.92 wt. %), and Mg# values (55-62). Moreover, all of these mafic dyke are alkaline and fall within the shoshonitic series (Fig. 4). The studied dolerites have distinct but near-identical chondrite- and primitive-mantle- normalized compositions (Fig. 5) that are enriched in LREEs, some of the LILEs (e.g., Rb, Ba, and Sr), and Pb. In addition, they also have negative Th, U, Nb and Ta anomalies, and some samples have negative Eu anomalies (Eu/Eu* = 0.51-0.96). By contrast, all samples studied, however, have sub-chondritic Nb/Ta ratios (12.5-18.0, where the chondritic ratio is 19.9  0.6; Munker et al., 2003) and record Zr/Hf fractionation with super-chondritic Zr/Hf ratios (44.8-97.2, where the chondritic ratio is 34.3 

0.3; Munker et al.,

2003).

5.3. Sr-Nd-Pb-Hf isotopes The Sr, Nd, and Pb isotopic compositions of representative dolerites were determined (Tables 3). These dykes have relatively constant initial 87Sr/86Sr

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ratios (0.7055-0.7057), and negative Nd (t) values (-12.5 to -11.9) that are indicative of a common source region. In addition, these mafic dykes yielded Nd model ages of 2.15-2.26 Ga (Table 3). This suggests that these samples have EM1-like Sr-Nd isotopic ratios (Hart, 1984; Zindler and Hart, 1986; Cai et al., 2004) that are also similar to Mesozoic mafic dykes from the NCC (Liu, 2004; Liu et al., 2008a, b, 2009a). This similarity is also demonstrated by the fact that all samples studied plot within the mantle array and shoshonitic field of an Nd (t) vs. (87Sr/86Sr) i diagram (Fig. 6). The dolerites have relatively constant Pb isotopic ratios (EM1-like) ((206Pb/204Pb) i = 16.45-16.51, (207Pb/204Pb) i = 15.44-15.51, and (208Pb/204Pb) i=

36.49-36.53) (Table3; Fig. 8b), similar to those of mafic dykes from the NCC

(Zhang et al., 2004; Xie et al., 2006; Liu et al., 2008a, b, 2009a), however, these differ from the composition of mafic dykes from the Yangtze Craton (Yan et al., 2003). The results of zircon Hf isotope analyses are shown in Table 4. A total of 17 spot analyses were undertaken on sample WC1, yielding uniform Hf (t) values of between -18.2 and -16.5 that correspond to TDM2 model ages of 2333-2226 Ma. A further 18 spot analyses on sample WC8 yield another narrow range of Hf (t) values, between -18.0 and -15.2 and TDM2 model ages of 2323-2142 Ma. A total of 16 spot analyses on sample FL2 yielded a relatively wide range of Hf (t) values (between -17.7 and -15.1) that correspond to TDM2 model ages of 2300-2136 Ma. Sixteen spot analyses on sample CC1 yielded a relatively wide

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range of Hf (t) values (-17.8 to -15.3) and TDM2 model ages of 2305-2149 Ma. The 16 spot analyses undertaken on sample HL1 yielded a narrow range of Hf (t) values between -17.7 and -15.2, and TDM2 model ages of 2300-2143 Ma. Finally, 16 spot analyses on sample FL2 yielded a narrow range of Hf (t) values between -17.8 and -15.1, and TDM2 model ages of 2300-2128 Ma. All of these Hf isotopic compositions are again consistent with an EM1-like signature (Yang et al., 2006).

6. Discussion Mesozoic intrusions are widespread in the Taihang gravity lineament, including gabbros in the Donggang, Fusan, Pingshan, Laiyuan, Badaling, and south Taihang areas (Cai et al., 2004; Zhang et al., 2004); 140-125 Ma diorite-monzonite complexes (Chen et al., 2004) of the Fusan area; Late Mesozoic gabbros and intermediate-felsic rocks of the tectonic-magmatic Taihang-Da Hinggan gravity lineament (Cai et al., 2003, 2004; Yang et al., 2004; Qin, 2005; Shen et al., 2015); magmatism in the Taihang mountains (Luo et al., 1997; Peng et al., 2004; Chen et al., 2005, 2006, 2007; Ying et al., 2010; Shen et al., 2015); alkaline rocks within the Taihang-Da Hinggan gravity lineament (Li and Yu, 1993; Cai et al., 2006); the Badaling area (Wang and Zhang, 2001); 125-127 Ma monzonites and diorites in the Dongye and Wu'an areas (Peng et al., 2004; Wang et al., 2006); the 115-135 Ma Pingshui diorites (Zhang et al., 2013); the 134-149 Ma volcanic rocks of the southern Da

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Hinggan gravity lineament, 135-145 Ma complexes in the Wanganzhen and the southern Dahe areas (Cai et al., 2003; Chen et al., 2003; Chen and Zhai, 2003); and the ~120 Ma calc-alkaline lamprophyres that lie above some intrusions in these areas (Chen et al., 2003). Previous investigation suggests that these Mesozoic intrusions formed from differing sources and have distinct origins (see the references in the introduction). Here, we use detailed geochronological and geochemical constraints to discuss the sourcing and origin of mafic dykes within the magmatic Taihang-Da Hinggan gravity lineament.

6.1. Timing of the mafic dykes Little previous research has been undertaken on mafic rocks within the tectonic-magmatic Taihang-Da Hinggan gravity lineament, although some studies have examined 164-120 Ma gabbros within the Donggang, Fusan and Ping shun, Laiyuan, Badaling, and south Taihang areas (Chen et al., 2003; Cai et al., 2004; Zhang et al., 2004; Tang et al., 2006; Ying et al., 2010). To date, no research has been undertaken on the Mesozoic mafic dykes in this area. The geochronological data (zircon U-Pb ages) summarized in Fig. 4 indicate that the mafic dykes were emplaced between 131.6  1.6 and 121.6  1.1 Ma, consistent with intrusion during the main stage of Early Cretaceous (164-120 Ma) magmatism within the tectonic-magmatic Taihang-Da Hinggan gravity lineament, as described above.

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6.2. Mantle source and crustal assimilation Mafic dykes studied contain lower SiO2 concentrations (50.12 -51.85 wt. %) than liquids produced from partial melting of any crustal rocks (i.e., granitic liquids; Rapp et al., 2003), suggesting that the dykes formed from mantlerather than crustal-derived magmas. This inference is also supported by the fact that these dykes have higher MgO concentrations (5.08-6.64 wt. %) and elevated Mg# values (55-62), although they contain fairly low concentrations of Cr (9.54-476 ppm) and Ni (6.63-165 ppm; Table 2). The high initial 87Sr/86Sr, negative εNd (t) (-12.5 to -11.9), and negative zircon εHf (t) (-18.2 to -15.1) values of the studied mafic dykes (Table 3,4; Fig. 7) are consistent with derivation from an enriched lithospheric mantle source, a hypothesis that is further supported by their EM1-like Pb isotopic compositions ((206Pb/204Pb) i = 16.45-16.51, (207Pb/204Pb) i = 15.44-15.51, and (208Pb/204Pb) i = 36.49-36.53; Table3; Fig.7b). Co-magmatic mafic and felsic rocks are often explained by assimilation and fractional crystallization (e.g., DePaolo, 1981; Devey and Cox, 1987; Marsh, 1989; Mingram et al., 2000), and the fact that the mafic dykes studied have positive Pb and negative Ti anomalies in primitive-mantle-normalized multi-element variation diagrams (Fig. 4b) suggests that some continental material was involved in the origin of the magmas that formed these units. This view is further supported by the fact that these dykes have much lower Ta/La ratios (0.01-0.02) than primitive mantle (e.g., Ta/La = 0.06: Wood et al., 1979). In addition, crustal contamination is

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likely to generate basaltic rocks with depleted Nb-Ta values and highly enriched Sr-Nd isotopic compositions (Guo et al., 2004). Crustal contamination is initially supported by the fact that the studied mafic dykes are characterized by negative Nb-Ta anomalies (Fig. 5b) and have high and constant initial 87Sr/86Sr

ratios and negative Nd (t) values (Table 3; Fig. 6). This suggests that

crustal contamination was possible in the formation of magmas that generated these dykes.

6.3. Partial melting and fractional crystallization The investigated dolerite dykes have La/Sm and Sm/Yb ratios (Table 2; Fig. 8a, b) that are consistent with magmas generated by relatively low to moderate partial melting (1.0 %-10 %) of a garnet lherzolite source. This is further supported by the high Ti/Y ratios of these dykes (238-474; Johnson, 1998). The low Cr, Ni and Co concentrations also support magma generation by the above-mentioned partial melting (Table 2). The positive correlations between MgO and Fe2O3, CaO, CaO/Al2O3, and Ni, and the negative correlations between MgO and SiO2, Al2O3, and Sr (not presented) are indicative of olivine, clinopyroxene, and hornblende fractionation, but also suggest that the magmas that formed these mafic dykes did not fractionate plagioclase, as also evidenced by the absence of significant negative Sr and Eu anomalies (Fig. 5a, b). The separation of Ti-bearing phases (e.g., rutile, ilmenite, and titanite) could also account for the negative Nb and Ta anomalies present within the

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primitive-mantle-normalized multi-element variation patterns of these dykes studied (Fig. 5b).

6.4. Genetic model The tectonic-magmatic Taihang-Da Hinggan gravity lineament lies between the NCC and the Erdos Plateau (Zhang et al., 2002), and is close to the Pacific tectonic belt. This belt contains numerous Mesozoic intrusions (Fig. 2; Cai et al., 2004) that have been studied previously (Zhang and Sun, 1988; Zhang, 1993; Niu et al., 1994; Deng, 1996, 2000; Xu et al., 1996; Wang and Zhao, 1997; Liu and Shi, 1998; Luo et al., 1999; Shao et al., 1999a, b, 2001, 2010; Wu and Sun, 1999; Hong et al., 2000; Wang and Zhang, 2001; Yan et al., 2000, 2001; Qian et al., 2002; Cai et al., 2003, 2004; Chen and Zhai, 2003; Chen et al., 2003, 2005, 2006, 2007; Peng et al., 2004; Zhang et al., 2004; Qin, 2005;

Yang et al., 2014; Shen et al., 2015), revealing that the rocks formed at

different stages of this magmatic event have differing characteristics. The intermediate to mafic rocks in the southern Taihang area were derived from partial melting of an enriched mantle reservoir, as were the early stage intermediate-mafic rocks in the northern Taihang area. In contrast, the intermediate-felsic rocks that formed during the middle stage of magmatism were sourced from the lower crust, and the alkaline intermediate-felsic rocks in this region were most likely sourced from the lower and middle crust. Nevertheless, the source and origin of these Mesozoic intrusions remains

19

debated. At present, at least four competing mechanisms can be envisaged to decipher the origin of the Mesozoic magmatism in the NCC: the subduction of the Yangtze Crust, the Siberian Craton and the ancient Pacific Plate beneath the NCC (Ge, 1999; Zhang et al., 2004, 2005; Chen et al., 2004); and the successive hybridism of foundered lower crust (Liu et al., 2008a, b). It is generally accepted that the Mesozoic magma activity within the NCC is related to the magma mixing between mantle- and ancient lower crust-derived magmas (Chen et al., 2002, 2003, 2004, 2005, 2006; Qian et al, 2002; Yang et al., 2004), however, further investigation is still needed. The mafic dykes studied herein are characterized by Pb isotopic characteristics (Table 3) that are similar to those of the Mesozoic mafic rocks within the NCC, but differ from those of the mafic rocks from the Yangtze Craton (Fig. 4, 5a), ruling out the involvement of Yangtze Craton lithospheric material. In addition, the subduction of the paleo-Pacific or Izanaqi Plate most likely released fluids and/or melts that metasomatized and modified the lithospheric mantle beneath the NCC (Chen et al., 2004). However, the Izanaqi Plate primarily moved towards the N or N-NE during the Cretaceous (Kimura et al., 1990), and there was no westward subduction of the paleo-Pacific Plate below the NCC prior to the Early Cretaceous. In addition, there is currently no evidence that the paleo-Pacific Plate contributed to the Mesozoic magma activity within the eastern NCC (Zhang et al., 2005). Moreover, investigations on Early Cretaceous mantle-derived rocks within the western NCC suggests that the

20

Late Mesozoic rocks in this region were derived from magmas sourced from enriched mantle sources unrelated to the subduction of the paleo-Pacific Plate (Wang et al., 2006; Ying et al., 2007; Liu et al., 2008a, b, 2009). Based on the above evidence, the origin of the studied dolerite dykes should relate to the NCC, and from the above discussion, the mafic dykes were derived from partial melting of an enriched mantle source; however, it is unclear how the enriched lithosphere source was formed beneath the NCC. It has been shown, that the enrichment time of the lithosphere beneath the study area (2.47-2.17 Ga) is similar to that of the NCC (2.54-1.49 Ga) (Cai et al., 2004). Here, we present a genetic model for the studied dolerite dykes involving foundering of the lower continental crust. Eclogite can be recycled into the mantle (Arndt and Goldstein, 1989; Kay and Kay, 1991; Jull and Kelemen, 2001; Gao et al., 2004), primarily as it has a higher density (by 0.2-0.4 gcm-3) than lithospheric mantle peridotite (Rudnick and Fountain, 1995; Jull and Kelemen, 2001; Anderson, 2006; Levander et al., 2006). Furthermore, eclogite also has lower melting temperatures than mantle peridotites (Yaxley, 2000; Kogiso et al., 2003; Sobolev et al., 2005); implying foundered silica-saturated eclogites can melt to produce silicic tonalite to trondhjemite melts that may variably hybridize with overlying mantle peridotite material. These reactions can produce an olivine-free pyroxenite that, if subsequently melted, will generate basaltic melts (Kogiso et al., 2003; Sobolev et al., 2005; Gao et al., 2008). The foundering model is supported by the voluminous coeval (238-102

21

Ma) magmatism (e.g., Taihang-Da Hinggan mountains, Yanshan area, Taihang-Yan mountains, Badaling, the NCC) (see the reference in introduction), as well as the large-scale mineralization in this region (Wang and Zhao, 1997; Dong, 2013), along with the occurrence of adakites in the northern Taihang mountains and the NCC (e.g., in the Dahenan, Laiyuan, Shouwangfei, Yumengshan, and Badaling areas; Xiong et al., 2011; Feng, 2012). Based on the above discussion, we thus propose the following model in which lower crustal delaminating coincided with mafic magmatism. At present, it is generally accepted that the collision between the Yangtze Craton and the NCC occurred during the Triassic (240-185 Ma), which resulted in a thickened crust and caused eclogitization of its lower parts (Zhang et al., 2002). This collision mechanism thus was used to explain the genetic model of some mafic dykes in Shandong province, China (Liu et al., 2008a, b, 2009). However, the samples studied were collected from the northern margin of the NCC, several hundred kilometers away from the Qinling-Dabie-Sulu Orogeny, which resulted from Triassic collision between the Yangtze Craton and the NCC. Even if lower crust foundering did take place at the northern margin of the NCC, combined with the above discussion, it is improper to link it with the collision between the Yangtze Craton and the NCC. By contrast, the collision between the Siberian Craton and the NCC (180-135 Ma; Ge, 1999) should be taken into account. Owing to the collision between the Siberian Craon and the NCC, a thickened and eclogitizatic lower crust formed beneath the study area, subsequently, this

22

eclogite was recycled into the mantle due to its higher density than lithosphere mantle peridotite. The silicic melts generated by the melting of these foundered eclogites reacted extensively with the overlying mantle peridotite, with the later (132-121 Ma) decompression melting of this hybridized lithosphere mantle, producing primary basaltic melts in an extensional setting, imparted in the subduction of the paleo-Pacific Plate (135-132 Ma; Fig.9b; Chen et al., 2005). Ultimately, the mafic dyke swarms were emplaced after fractional crystallization during ascent of the primary basaltic melts (Fig. 9c). 7. Mesozoic delamination timing and range in the NCC form East to West Special attention has been paid to delamination (Wu et al., 2003, 2005, 2006; Gao et al., 1992, 1998a, b, c, 2002, 2003, 2004, 2008; Liu et al., 2005; Xu et al., 2004, 2006; Lin and Wang, 2006; Yang et al., 2007; Deng et al., 2007; Wang et al., 2007; Yang and Li, 2008; Liu et al., 2006, 2008a, b, 2009a, b, c, 2010, 2012, 2013a, b, c) since it was proposed (Bird, 1978, 1979). Owing to the instability of gravity, delamination leads to sink of the lithospheric mantle and lower continental crust into the asthenosphere and concomitant upwelling of the asthenosphere onto the crust-mantle boundary (Gao and Jin, 2007; Gao et al., 2009). Normally, this process results in exchange between the lower rust, the lithospheric mantle and the asthenosphere and cause magmatism and uplift, extension and collapse of mountains, thinning of lithosphere as well as formation of sag basin (Gao and Jin, 2007). As this model can explain many geological phenomena in the NCC (e.g., the widespread high Mg adakite; the

23

eclogite of lower crust existing in Mesozoic basalt, peridotite and pyroxene; the episodic magmatism; the relatively low seismic wave velocity and Poisson's ratio; absence of Archean mantle remains) very well. Currently, which has been considered as the main model for the Mesozoic destruction (peak period is 125 Ma; Zhu et al., 2011) of the NCC (Deng et al., 1994, 1996; Wu et al., 2008; Gao et al., 2009), accordingly, delamination is common in the NCC, although there are still some phenomena that cannot be explained (Menzies et al., 2007; Wu et al., 2008). Nevertheless, Mesozoic delamination timing and range in the NCC from east to west still unclear. Based on the existing studies, the above issues will be discussed as follows. At present, except some studies focused on Mesozoic igneous rocks (e.g., Sulu Orogenic Belt 119-120 Ma, Jiaobei 122-127 Ma, Tancheng-Lujiang Fault 124.9-129.6 Ma, Jiaodong 122-123 Ma, Dalian 210 Ma, Songliao Basin 262 Ma, and Luxi 143-144 Ma mafic dykes; Jiaobei 123.6 Ma, and Wulatezhongqi in Inner Mongolia 291 Ma adakites; Jiaodong 114-122 Ma, Sulu Orogenic Belt 120-127 Ma alkaline rocks; Sulu Orogenic Belt 127 Ma intrusive complexes; Luo et al., 2007; Liu et al., 2008a, b, 2009a, b, c, 2010, 2012, 2013a, b, c) in the NCC, suggesting that the foundering in the NCC from east to west mainly occurred between late Jurassic and Cretaceous, and the time frame is concentrated between 144 Ma and 120 Ma. Further study and discussion on this field thus is needed.

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8.

Conclusions New geochronological, geochemical, and Sr-Nd-Pb-Hf isotopic data for

mafic dykes of northern Taihang gravity lineament allow us to reach the following conclusions. (1) The mafic dykes were intruded during the Cretaceous as evidenced by six new zircon U-Pb ages, of between 131 ± 1.6 and 121.6 ± 1.1 Ma. (2) All of the dykes are alkaline and shoshonitic, being enriched in the LREE, some of the LILE (e.g., Rb, Ba, and Sr), Pb, Th and U, and depleted in Nb, Ta, and sometimes Eu. They have high initial

87Sr/86Sr

ratios

(0.7055-0.7057), negative εNd (t) values (-12.5 to -11.9), relatively constant Pb isotopic ratios ((206Pb/204Pb) i = 16.45-16.51, (207Pb/204Pb) i = 15.44-15.51, (208Pb/204Pb) i = 36.49-36.53), negative εHf (t) values of between -18.2 and -15.1, and old Nd and Hf model ages (2.47-2.13Ga). These data suggest the magmas that formed these dykes were generated by low to moderate degree partial melting (1.0 %-10 %) of an EM1-like garnet Iherzolite mantle source material. Meanwhile, fractionation of olivine, clinopyroxene, and hornblende and

low to moderate degree crustal contamination occurred during magma

ascent. (3) The 132-121 Ma mafic dyke swarms of the northern Taihang gravity lineament formed as a result of asthenospheric upwelling associated with foundering of eclogite from lower thickened crust in a tectonic setting influenced by the continual collision between the Siberian Craton and the

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NCC. (4) Mesozoic the foundering in the NCC from east to west mainly occurred between late Jurassic and Cretaceous, and the time frame is concentrated between 144 Ma and 120 Ma.

Acknowledgments The authors thank Dr. Shuqin Yang for assistance during XRF analyses, Prof. Liang Qi and Ms. Jing Hu for assistance during ICP-MS analyses, the analyst for assistance during TIMS Sr-Nd-Pb isotopic analyses, and Profs Xiaoming Li and Honglin Yuan for assistance during LA-ICP-MS U-Pb dating and Hf isotopic analyses. This study was supported by the National Natural Science Foundation of China (grants 41373028 and 41573022).

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Figure captions Fig.1. The simplified geological setting of the Taihang-Da Hinggan gravity lineament. Fig. 2. Geological map of the study areas and the distribution of the mafic dykes across this region of China. Fig. 3. Zircon LA-ICP-MS U-Pb concordia diagrams for the studied mafic dykes within the area of the Taihang-Da Hinggan gravity lineament. Fig. 4. Total alkali vs. silica (TAS) plot for mafic dykes within the area of the Taihang-Da Hinggan gravity lineament. All major element data have been recalculated to 100 % on an anhydrous basis (after Middlemost, 1994; Le Maitre, 2002). Fig.5. Chondrite-normalized REE and primitive-mantle-normalized multi-element variation diagrams for the studied mafic dykes within the area of the Taihang-Da Hinggan gravity lineament; these values are normalized to the chondrite and primitive mantle compositions of Sun and McDonough (1989). Fig. 6. Diagram showing variations in initial 87Sr/86Sr vs. Nd (t) for the investigated mafic dykes within the area of the Taihang-Da Hinggan gravity lineament. Also shown are the compositions of Mesozoic mafic rocks from the North China Craton (Liu et al., 2008a, b, 2009a) and mafic rocks from the Yangtze Craton (Chen et al., 2001; Li et al., 2004). Fig. 7. Variations in 208Pb/204Pb and 207Pb/204Pb vs. 206Pb/204Pb within the mafic

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dykes from the area of the Taihang-Da Hinggan gravity lineament. Also shown are I-MORB (Indian MORB) and P & N-MORB (Pacific and North Atlantic MORB), OIB, and NHRL fields, and a 4.55 Ga geochron after Barry and Kent (1998), Zou et al. (2000), and Hart (1984), respectively. The North China Craton data are from Zhang et al. (2004) and Xie et al. (2006), and data of mafic rocks of the Yangtze Craton are from Yan et al. (2003). Fig. 8. Variations in La/Sm vs. La and Sm/Yb vs. Sm compositions of the samples analyzed during this study, and melt curves and lines derived from the non-modal batch melting equations of Shaw (1970). Melt curves are shown for spinel lherzolite (with mode and melt mode compositions of ol0.600 + opx0.200 + cpx0.100 + gt0.100 and ol0.030 + opx0.160 + cpx0.880 + sp0.110, respectively; Walter, 1998). Mineral/matrix partition coefficients and the composition of the DMM are from McKenzie and O’Nions (1991, 1995). Primitive mantle, and N-MORB and E-MORB compositions are from Sun and McDonough (1989). Tick marks on each curve or line correspond to changing degrees of partial melting of a given mantle source. Fig. 9. Tectonic evolution of the study area of the Taihang-Da Hinggan gravity lineament (Liu et al., 2008a, b, 2009a). (a) 240-185 Ma: collision of the Yangtze Block and NCC resulted in thickening of the lithosphere (mantle and lower crust) and eclogitization of the lower thickened crust; (b) 185-165 Ma: delamination of the eclogitic lower crust occurred, followed by the generation of silicic melts via the melting of foundered eclogite, which reacted

49

extensively with overlying mantle peridotite; (c) 132-121 Ma: decompression melting of the hybridized lithospheric mantle produced the parent magmas to the mafic dykes.

50

51

52

53

54

55

56

57

58

Table captions Table 1.

Zircon LA-ICP-MS U-Pb isotopic data for samples from the dolerites in the area of the Taihang-Da Hinggan gravity lineament.

LWM01 Spot Th U 1 457 451 2 4085 2698 3 547 565 4 124 49.5 5 276 147 6 170 156 7 69.3 55.2 8 163 148 9 200 179 10 133 127 11 303 85.5 12 61.3 63.1

Isotopic 207Pb/206Pb

ratios 1s ##### ##### ##### ##### ##### ##### ##### ##### ##### ##### ##### #####

Pb 408 187 14.9 16.5 29.4 26.6 29.9 24.1 28.6 22.1 63.3 8.63

Th/U 1.01 1.51 0.97 2.50 1.88 1.09 1.26 1.10 1.12 1.05 3.55 0.97

238U/232Th

0.46 1.51 0.63 2.5 1.88 1.09 0.46 0.47 0.53 0.37 3.55 0.84

0.0517 0.0517 0.0506 0.0519 0.0518 0.0516 0.0517 0.0518 0.0507 0.0515 0.0515 0.0508

207Pb/206Pb

ratios 1s

Isotopic

Age (Ma) 207Pb/235U

1s 0.0064 0.0067 0.0033 0.0064 0.0055 0.0060 0.0066 0.0063 0.0035 0.0064 0.0064 0.0033

206Pb/238U

207Pb/235U

0.2283 0.2278 0.2256 0.2264 0.2274 0.2281 0.2283 0.2272 0.2258 0.2288 0.2294 0.2236

0.0335 0.0335 0.0336 0.0331 0.0333 0.0334 0.0334 0.0333 0.0335 0.0336 0.0335 0.0336

1s ##### ##### ##### ##### ##### ##### ##### ##### ##### ##### ##### #####

207Pb/206Pb

1s

206Pb/238U

0.0044 0.0041 0.0052 0.0066 0.0046 0.0035 0.0036 0.0066 0.0042 0.0058 0.0058 0.0054 0.0057

0.0316 0.0315 0.0316 0.0315 0.0314 0.0313 0.0316 0.0312 0.0312 0.0314 0.0317 0.0315 0.0314

1s 0.0003

WJZ02 Spot

Th

U

Pb

Th/U

238U/232Th

1 2 3 4 5 6 7 8 9 10 11 12 13

457 68.5 198 375 429 3587 66.8 811 222 457 190.7 747 84.7

451 23.9 12.6 73.2 204 1399 23.4 640 120 451 11.8 403 30.3

396 14.2 19.3 62.7 55.1 210 13.6 245 15.3 396 18.4 53.3 17.0

1.01 2.87 15.65 5.13 2.11 2.56 2.86 1.27 1.86 1.01 16.10 1.85 2.79

1.38 5.13 1.98 2.29 2.18 2.66 1.36 1.01 1.33 1.85 2.36 2.03 1.28

0.0521 0.0501 0.0544 0.0505 0.0527 0.0506 0.0519 0.0499 0.0523 0.0519 0.0523 0.0506 0.0511

0.0018 0.0017 0.0019 0.0021 0.0018 0.0016 0.0016 0.0017 0.0017 0.0020 0.0020 0.0019 0.0019

0.2268 0.2174 0.2372 0.2194 0.2281 0.2182 0.2265 0.2149 0.2248 0.2244 0.2282 0.2200 0.2215

Isotopic

ratios 1s

207Pb/235U

1s

206Pb/238U

0.0016

0.1447

0.0024

0.0212

MJZ02 Spot

Th

U

Pb

Th/U

238U/232Th

207Pb/206Pb

1

8136

1701

217

4.78

5.72

0.0494

1s 42 41 15 38 39 39 39 38 16 38 38 16

207Pb/235U

206Pb/238U

209 208 207 207 208 209 209 208 207 209 210 205

1s 5 6 3 5 5 5 5 5 3 5 5 3

212 212 213 210 211 212 212 211 212 213 212 213

1s 2 3 2 3 2 2 3 3 3 3 3 2

1s

207Pb/206Pb

1s

207Pb/235U

1s

206Pb/238U

1s

0.0004 0.0004 0.0005 0.0005 0.0004 0.0004 0.0004 0.0004 0.0004 0.0005 0.0005 0.0005 0.0005

288 201 388 219 315 220 281 191 297 281 297 223 244

22 21 25 42 23 17 16 80 21 34 32 31 33

208 200 216 201 209 200 207 198 206 206 209 202 203

4 3 4 5 4 3 3 6 4 5 5 4 5

200 200 201 200 199 199 201 198 198 199 201 200 199

3 3 3 3 3 3 3 3 3 3 3 3 3

207Pb/206Pb

1s

207Pb/235U

1s

206Pb/238U

1s

169

17

137

2

135

2

270 273 223 281 276 269 270 274 225 261 261 232

Age (Ma)

Age (Ma)

59

2 3 4 5 6 7 8 9 10 11 12

1980 93.7 3876 1471 3630 2893 1265 290 274 374 2510

681 73.5 678 668 742 2120 568 73.9 225 198 688

68.6 5.52 102 46.2 99.8 81.1 33.6 22.1 10.2 11.9 57.7

2.91 1.28 5.72 2.20 4.89 1.37 2.23 3.92 1.22 1.89 3.65

2.2 4.89 1.37 2.23 1.22 1.89 3.65 1.01 3.88 0.31 0.38

0.0499 0.0483 0.0525 0.0493 0.0493 0.0514 0.0487 0.0500 0.0491 0.0488 0.0518

0.0017 0.0013 0.0017 0.0022 0.0027 0.0028 0.0016 0.0018 0.0022 0.0018 0.0018

0.1473 0.1421 0.1586 0.1415 0.1458 0.1528 0.1427 0.1491 0.1446 0.1449 0.1520

0.0031 0.0034 0.0026 0.0058 0.0066 0.0079 0.0025 0.0037 0.0052 0.0034 0.0033

0.0214 0.0213 0.0219 0.0208 0.0215 0.0216 0.0212 0.0216 0.0213 0.0216 0.0213

Isotopic

ratios 1s

207Pb/235U

1s

206Pb/238U

1s

0.00544 0.005 0.00427 0.00303 0.00681 0.00234 0.00749 0.00441 0.00275 0.00357

0.00192 0.00187 0.00196 0.00191 0.00184 0.00198 0.00192 0.00186 0.00187 0.00186

MJZ03 Spot

Th

U

Pb

Th/U

238U/232Th

207Pb/206Pb

1 2 3 4 5 6 7 8 9 10

312 142 669 116 139 215 335 358 400 275

113 188 358 102 55.6 105 210 268 271 158

241 3.6 53.6 19.1 56.9 0.4 0.8 0.9 152 1.9

2.77 0.76 1.87 1.14 2.51 2.04 1.59 1.34 1.47 1.74

1.59 2.13 2.22 2.23 0.65 2.3 1.87 2.01 1.06 2.65

0.04724 0.05079 0.04697 0.04667 0.04804 0.0471 0.05161 0.05297 0.04702 0.04969

0.0208 0.0197 0.016 0.0117 0.0272 0.0088 0.0286 0.0175 0.0109 0.0141

0.01254 0.01307 0.01269 0.01231 0.01217 0.01285 0.01364 0.01358 0.01213 0.01277

JY01 Spot

Isotopic Th

U

Pb

Th/U

238U/232Th

207Pb/206Pb

ratios 1s

207Pb/235U

1s

206Pb/238U

1 2 3 4 5 6 7 8 9 10

806 2573 952 474 164 457 454 587 415 686

137 2090 27.7 36.5 58.0 451 86.7 38.7 293 248

292 302 422 240 9.8 396 224 217 179 199

5.88 1.23 34.36 12.99 2.82 1.01 5.23 15.15 1.42 2.77

2.76 2.75 2.77 2.77 2.77 2.76 2.77 2.77 2.75 2.76

0.0498 0.0482 0.0524 0.0494 0.0492 0.0515 0.0486 0.0502 0.0494 0.0486

0.0016 0.0014 0.0018 0.0021 0.0026 0.0027 0.0017 0.0018 0.0023 0.0017

0.1475 0.1423 0.1585 0.1416 0.1457 0.1527 0.1428 0.1492 0.1447 0.1448

0.0032 0.0035 0.0027 0.0057 0.0065 0.0079 0.0026 0.0038 0.0053 0.0035

0.0215 0.0214 0.0218 0.0207 0.0216 0.0217 0.0213 0.0217 0.0214 0.0215

Isotopic Th/U 238U/232Th 207Pb/206Pb 4.14 4.14 0.0524

HM03 Spot

Th

U

Pb

1

1459

352

52.9

ratios 1s 0.003

0.0003 0.0003 0.0003 0.0003 0.0004 0.0003 0.0003 0.0003 0.0003 0.0003 0.0003

192 113 306 160 162 257 135 195 155 136 275

24 66 17 101 75 126 19 31 55 29 25

140 135 150 134 138 144 135 141 137 137 144

3 3 2 5 6 7 2 3 5 3 3

136 136 140 133 137 138 135 138 136 137 136

2 2 2 2 2 2 2 2 2 2 2

207Pb/206Pb

1s

207Pb/235U

1s

206Pb/238U

1s

0.0001 0.0001 9E-05 8E-05 0.0002 5E-05 0.0001 0.0001 7E-05 8E-05

61 231 48 32 101 54 268 328 50 181

611 563 486 358 842 292 857 500 340 426

13 13 13 12 12 13 14 14 12 13

5 5 4 3 7 2 8 4 3 4

12.4 12.0 12.6 12.3 12.0 12.8 12.4 12.0 12.0 12.0

0.9 0.8 0.6 0.5 1 0.3 0.9 0.7 0.5 0.5

1s

207Pb/206Pb

1s

207Pb/235U

1s

206Pb/238U

1s

0.0003 0.0003 0.0004 0.0003 0.0004 0.0003 0.0003 0.0004 0.0003 0.0003

192 114 306 160 162 257 135 195 155 136

25 32 19 66 73 90 20 28 56 31

140 135 149 134 138 144 136 141 137 137

3 3 2 5 6 7 2 3 5 3

137 136 139 132 137 138 136 139 136 137

2 2 3 2 2 2 2 3 2 2

207Pb/206Pb

1s

207Pb/235U

1s

206Pb/238U

1s

303

78

117

5

124

2

Age (Ma)

Age (Ma)

Age (Ma) 207Pb/235U

0.1226

1s 0.0057

206Pb/238U

0.0194

60

1s 3E-04

2 3 4 5 6 7 8 9 10 11 12

628 865 569 714 99.3 449 2608 534 1543 1263 640

188 321 160 346 48.2 445 751 218 364 441 241

24.5 32.0 26.1 49.8 5.1 387 73.3 17.7 64.1 113 46.2

3.34 2.69 3.55 2.07 2.06 1.01 3.47 2.45 4.24 2.86 2.66

XHH01 Spot

Th

U

Pb

Th/U

1 2 3 4 5 6 7 8 9 10 11

457 208 71.3 358 413 583 178 263 522 171 236

450 106 61.2 227 351 403 107 53.4 132 140 123

398 90.6 12.6 26.6 20.9 54.0 10.8 18.8 157 8.87 16.9

1.01 1.96 1.16 1.58 1.18 1.45 1.67 4.93 3.95 1.22 1.92

3.34 2.12 2.12 2.12 2.12 2.12 2.13 2.12 2.13 2.12 2.12

0.0516 0.003 0.0519 0.003 0.0461 0.0027 0.0518 0.003 0.0525 0.003 0.0524 0.003 0.0526 0.003 0.0523 0.003 0.0522 0.002 0.0521 0.002 0.0523 0.003 Isotopic

0.1232 0.1253 0.1254 0.1236 0.1248 0.1235 0.1235 0.1229 0.1232 0.1226 0.1221

238U/232Th

207Pb/206Pb

ratios 1s

207Pb/235U

1.58 1.57 1.58 1.58 1.58 1.58 1.58 1.57 1.58 1.56 1.56

0.0554 0.0517 0.0518 0.0462 0.0519 0.0526 0.0525 0.0525 0.0524 0.0521 0.0522

0.0028 0.0027 0.0025 0.0027 0.0029 0.0028 0.0027 0.0028 0.0026 0.0024 0.0024

0.1225 0.1233 0.1254 0.1253 0.1235 0.1247 0.1236 0.1234 0.1289 0.1233 0.1225

0.0059 0.0058 0.0071 0.0056 0.0056 0.0055 0.0055 0.0062 0.0061 0.0061 0.0056

0.0187 4E-04 0.0196 3E-04 0.0193 0.0003 0.0196 0.0003 0.0189 3E-04 0.0191 3E-04 0.0198 3E-04 0.0192 3E-04 0.0191 3E-04 0.0196 3E-04 0.0195 3E-04

268 281 277 307 303 312 299 294 290 299

71 78 97 73 73 73 74 87 84 86 76

118 120 120 118 119 118 118 118 118 117 117

5 5 6 5 5 5 5 6 6 6 5

119 125 123 125 121 122 126 123 122 125 124

3 2 2 2 2 2 2 2 2 2 2

Age (Ma) 1s

206Pb/238U

1s

207Pb/206Pb

1s

207Pb/235U

1s

206Pb/238U

1s

0.0056 0.0058 0.0058 0.0072 0.0057 0.0055 0.0056 0.0054 0.0063 0.0062 0.0061

0.0195 0.0186 0.0195 0.0194 0.0195 0.0188 0.0192 0.0197 0.0193 0.0192 0.0195

0.0003 0.0004 0.0003 0.0003 0.0004 0.0003 0.0003 0.0003 0.0004 0.0003 0.0003

428 272 277 5 281 312 307 307 303 290 294

74 69 78 99 66 71 75 72 74 86 86

117 118 120 120 118 119 118 118 123 118 117

5 5 5 6 5 5 5 5 6 6 6

124 119 124 124 124 120 123 126 123 123 124

2 3 2 2 3 2 2 2 3 2 2

61

Table 2. Major (wt. %) and trace (ppm) element compositions of the dolerites within the area of the Taihang-Da Hinggan gravity lineament. Sample

SiO2

TiO2

Al2O3

Fe2O3

MnO

MgO

CaO

K2O

Na2O

P2O5

LOI

Total

Mg#

LWM01 LWM02 LWM03 LWM04 LWM05 LWM06 LWM07 WJZ01 WJZ02 WJZ06 MJZ03 MJZ04 MJZ05 MJZ11 MJZ18 MJZ25 MJZ27 MJZ28 MJZ31 MJZ32 MJZ35 MJZ36 MJZ42 MJZ44 MJZ46 JY03 JY07 JY12 JY13 JY14 JY15 HM01 HM03 XHH02 XHH03 XHH04 XHH05

49.47 49.29 49.36 48.68 50.90 49.46 50.63 50.55 47.65 48.54 49.43 48.97 49.22 47.55 49.59 49.89 50.13 50.18 50.45 49.98 50.16 50.20 49.97 50.43 51.57 49.16 48.58 49.41 49.68 49.34 49.15 47.70 46.98 48.87 48.48 49.34 49.53

0.95 0.97 0.93 1.15 0.91 0.89 1.04 0.68 0.54 0.63 0.89 0.87 0.85 0.98 1.33 1.30 1.28 1.31 1.29 1.29 1.32 1.29 1.24 1.11 1.09 1.17 1.17 1.19 1.15 1.16 0.67 2.87 2.71 1.31 1.22 1.24 1.29

14.91 14.79 14.75 14.68 14.56 14.46 13.62 14.63 14.06 16.38 13.96 13.89 13.89 14.27 13.14 13.22 13.18 13.17 12.85 13.13 13.01 13.06 13.20 13.40 13.22 14.31 14.25 14.32 13.90 14.41 14.93 18.26 17.29 12.92 14.47 12.83 12.95

12.93 13.06 13.22 13.07 12.51 13.13 13.01 10.38 10.87 10.50 13.92 13.79 13.69 14.03 14.96 15.02 15.18 15.25 15.24 14.89 15.39 15.31 14.88 14.50 14.16 14.87 14.61 14.67 14.55 14.61 12.59 12.11 11.95 15.40 14.74 13.89 15.16

0.17 0.17 0.18 0.19 0.17 0.17 0.17 0.16 0.15 0.14 0.20 0.20 0.20 0.20 0.20 0.20 0.20 0.20 0.20 0.20 0.20 0.20 0.19 0.20 0.19 0.19 0.20 0.19 0.20 0.19 0.25 0.03 0.03 0.19 0.20 0.19 0.20

6.09 6.32 6.47 6.53 6.63 6.86 6.16 8.07 11.11 7.78 7.04 7.08 7.15 8.19 6.13 6.17 6.06 6.13 6.02 5.97 6.12 6.11 6.37 6.10 5.88 6.25 6.26 6.09 6.58 6.18 7.43 6.58 8.09 6.67 6.15 5.68 6.05

9.53 9.04 9.83 9.08 9.19 10.40 10.29 10.59 9.81 10.35 11.20 11.13 11.11 8.91 10.59 10.48 10.50 10.46 9.53 10.25 9.83 9.69 10.56 10.41 9.91 8.54 9.67 9.55 9.34 9.24 9.01 2.45 2.49 9.46 9.71 10.67 10.16

1.83 1.87 1.84 1.84 1.85 1.76 1.85 1.82 1.85 1.84 1.94 1.98 1.96 2.08 1.93 1.95 1.93 1.94 1.96 1.94 1.93 1.95 1.92 1.93 1.92 1.96 1.97 1.96 1.95 1.93 1.97 2.46 2.53 1.98 1.96 1.94 1.96

3.34 3.38 2.78 3.41 2.86 2.79 2.28 1.94 1.77 2.14 1.56 1.67 1.64 1.87 1.85 1.73 1.62 1.46 1.52 1.81 1.71 1.83 1.52 1.56 1.42 1.85 1.78 1.69 1.58 1.46 1.88 3.45 3.39 2.46 2.54 2.46 2.35

0.26 0.26 0.26 0.27 0.25 0.22 0.14 0.15 0.12 0.14 0.08 0.08 0.08 0.09 0.12 0.11 0.12 0.12 0.13 0.12 0.13 0.12 0.11 0.12 0.14 0.19 0.19 0.19 0.18 0.19 0.15 1.05 1.17 0.13 0.19 0.12 0.12

0.44 0.37 0.32 0.97 0.39 0.25 0.67 0.87 1.35 1.21 0.23 0.32 0.31 0.92 0.31 0.19 0.15 0.16 0.33 0.36 0.14 0.18 0.19 0.15 0.14 0.32 0.45 0.35 0.36 0.82 1.25 2.33 2.28 0.26 0.21 0.82 0.15

99.92 99.52 99.94 99.87 100.22 100.39 99.86 99.84 99.28 99.65 100.45 99.98 100.10 99.09 100.15 100.26 100.35 100.38 99.52 99.94 99.94 99.94 100.15 99.91 99.64 98.81 99.13 99.61 99.47 99.53 99.28 99.29 98.91 99.65 99.87 99.18 99.92

62 60 62 60 62 64 64 69 67 68 64 64 64 58 61 61 60 60 58 60 58 60 61 63 65 59 62 62 61 61 64 54 60 60 62 66 62

62

Table 3. S-Nd-Pb isotopic compositions of representative dolerites within the area of the Taihang-Da Hinggan gravity lineament. Ga

Ba

16.5 15.4 16.9 15.7 16 15.6 17.4 13.9 13.5 15.6 16.8 16.2 17.4 20.4 19.4 20.1 19 19.7 19.7 20.9 18.7 19.3 18.9 20.1 18.8 21 21.4 19.8 19.4 19.5 15.2 36.1 36.8 18.8 21.1 17.1 17.4

304 456 254 200 389 105 236 69.5 281 42.8 67.4 48.1 71.3 146 37.1 33.8 45.5 53.5 70.3 77.5 61.7 69.8 33.4 42.6 42.7 91.7 37.9 54.7 58.6 108 93.3 718 743 349 69.9 96.8 69.6

Rb

Sr

Y

22.3 252 21.7 33.5 242 19.8 17.7 271 20.4 15.2 240 19.9 31.6 262 20.6 6.02 242 18.4 13.8 257 25.8 3.72 196 12.3 15.7 185 10.4 2.53 240 12.3 10.4 138 20.2 9.51 133 19.6 14.1 138 20.5 33.4 135 29.2 1.5 146 28.1 1.61 155 28.1 1.72 130 27 2.43 140 27.5 9.31 147 28.2 4.93 133 29.9 7.82 141 26.6 2.11 133 28.1 1.53 148 25.6 2.21 161 27.6 2.14 161 30.9 6.12 290 23.4 1.91 308 23.9 2.72 287 23.9 3.71 253 23.6 5.22 295 23.3 4.04 204 15.3 88.8 1857 93.5 93.5 1962 77.8 22.4 135 28.1 4.32 305 23.8 6.14 165 24.8 3.72 146 27.9

Zr

Hf

Nb

Ta

Th

U

Pb

La

Ce

Pr

Nd

Sm

Eu

Gd

Tb

Dy

Ho

Er

Tm

Yb

Lu

74 71 74 71 76 60 108 45 37 46 59 58 59 69 91 92 90 86 94 98 88 91 83 89 103 86 88 88 86 85 34 520 524 87 91 81 90

1.93 1.81 1.83 1.94 1.82 1.52 2.83 1.22 1.06 1.22 1.73 1.71 1.72 1.92 2.53 2.51 2.54 2.45 2.43 2.62 2.54 2.53 2.21 2.33 3.04 2.51 2.44 2.61 2.42 2.43 1.07 13.5 13.3 2.52 2.34 2.41 2.52

3.83 3.62 3.61 3.53 3.61 3.63 4.35 2.52 2.05 2.43 2.81 2.72 2.83 3.25 4.24 4.42 4.03 4.12 4.33 4.32 4.15 4.13 3.91 3.92 4.73 4.42 4.31 4.24 4.06 4.32 1.63 20.4 19.5 4.14 4.31 4.06 3.71

0.23 0.24 0.22 0.21 0.22 0.23 0.32 0.23 0.14 0.13 0.24 0.22 0.23 0.23 0.32 0.31 0.31 0.33 0.32 0.32 0.31 0.33 0.24 0.33 0.31 0.32 0.33 0.32 0.31 0.32 0.13 1.71 1.82 0.32 0.33 0.32 0.31

0.52 0.52 0.56 0.53 0.53 0.47 1.72 0.41 0.36 0.43 0.68 0.72 0.69 0.79 1.17 1.21 1.21 1.21 1.23 1.32 1.19 1.19 1.06 1.14 1.49 1.03 1.04 0.97 0.97 1.05 0.29 17.9 18.3 1.21 1.04 1.11 1.29

0.2 0.16 0.11 0.11 0.1 0.09 0.35 0.06 0.04 0.05 0.19 0.22 0.2 0.26 0.27 0.28 0.28 0.26 0.32 0.33 0.28 0.27 0.27 0.26 0.34 0.22 0.16 0.25 0.23 0.29 0.05 5.61 4.76 0.25 0.35 0.21 0.27

5.15 3.21 3.18 4.22 4.24 4.17 4.15 1.21 2.13 1.75 2.28 2.16 3.24 3.28 2.33 3.09 15.3 1.82 1.64 1.73 1.42 4.11 13.3 2.19 6.08 4.22 2.31 1.64 1.52 2.18 2.25 3.23 4.14 2.15 3.06 4.12 3.14

17.3 15.3 15.1 14.2 14.5 11.6 14.3 7.81 10.5 9.16 8.71 8.53 8.62 13.1 11.2 11.6 10.4 10.8 12.1 11.3 11.4 11.4 10.4 10.9 12.3 14.1 13.7 14.2 13.1 16.8 8.62 104 88.6 9.14 9.39 8.15 8.93

35.3 32.3 32.2 30.5 30.6 24.6 30.2 16.9 14.4 17.1 14.9 14.4 15.3 22.4 21.2 22.5 20.6 21.3 23.5 23.3 22.2 21.6 20.6 22.1 25.2 29.9 30.3 31.7 29.4 34.8 16.5 226 201 19.7 22.3 18.4 20.2

4.42 4.18 4.19 4.15 4.11 3.42 3.88 2.28 1.89 2.19 2.21 2.17 2.22 2.76 2.83 3.15 3.04 3.13 3.23 3.19 3.06 3.03 2.93 3.12 3.25 4.13 3.82 3.96 3.83 4.4 2.24 27.4 24.3 2.63 3.03 2.51 2.81

19.1 17.5 17.9 17.1 17.8 14.6 16.6 10.5 8.04 9.91 10.3 10.2 9.85 14.2 14.3 13.4 14.2 13.7 14.6 14.6 14.2 14.4 13.3 13.8 16.1 18 17.6 18 17.7 19.2 9.33 117 107 11.7 14.2 11.4 12.4

3.66 3.79 3.72 3.91 3.72 3.23 3.98 2.42 1.95 2.22 2.55 2.69 2.54 3.62 3.8 3.73 3.98 3.69 3.89 3.78 3.8 3.67 3.59 3.57 4.25 4.49 4.52 4.54 4.46 4.53 2.38 27.3 23.6 3.51 3.86 3.33 3.71

1.16 1.11 1.12 1.09 1.17 1.04 1.06 0.78 0.63 0.66 0.86 0.88 0.88 1.33 1.21 1.24 1.24 1.19 1.31 1.26 1.26 1.22 1.17 1.16 1.51 1.46 1.36 1.46 1.35 1.58 0.84 7.09 6.25 1.07 1.42 1.15 1.32

3.68 3.82 3.75 3.74 3.67 3.29 3.52 2.51 2.03 2.3 3.41 3.51 3.34 5.12 4.62 4.52 4.77 4.32 4.94 4.87 4.62 4.55 4.15 4.44 5.41 4.84 4.52 5.01 4.69 4.84 2.87 24.9 20.9 4.56 4.65 4.08 4.57

0.51 0.56 0.57 0.55 0.54 0.49 0.52 0.35 0.27 0.32 0.56 0.57 0.55 0.77 0.76 0.75 0.77 0.72 0.78 0.81 0.71 0.75 0.69 0.73 0.89 0.7 0.68 0.75 0.67 0.72 0.43 3.37 2.78 0.73 0.69 0.68 0.76

3.51 3.49 3.56 3.51 3.42 3.12 3.41 2.21 1.81 2.16 3.43 3.76 3.64 4.82 5.1 5.05 4.89 4.77 4.83 4.99 4.82 4.84 4.36 4.71 5.61 4.31 4.32 4.54 4.16 4.39 2.78 19.6 15.6 4.63 4.21 4.33 4.86

0.78 0.77 0.77 0.76 0.74 0.67 0.72 0.49 0.4 0.47 0.77 0.84 0.79 1.06 1.12 1.11 1.08 1.06 1.12 1.14 1.06 1.11 0.98 1.05 1.32 0.94 0.94 1.01 0.95 0.97 0.59 3.79 3.15 1.06 0.95 0.98 1.11

2.21 2.14 2.24 2.18 2.22 1.99 2.21 1.45 1.17 1.29 2.23 2.39 2.21 3.05 3.1 3.13 3.16 3.09 3.21 3.22 3.13 3.16 2.82 2.94 3.71 2.68 2.63 2.8 2.63 2.65 1.75 9.47 7.89 3.02 2.56 2.99 3.17

0.33 0.33 0.33 0.34 0.32 0.31 0.31 0.22 0.17 0.2 0.34 0.36 0.33 0.43 0.46 0.46 0.47 0.44 0.47 0.49 0.47 0.46 0.42 0.43 0.53 0.40 0.39 0.43 0.34 0.34 0.26 1.28 1.09 0.45 0.39 0.43 0.48

2.08 2.09 2.17 2.15 2.09 1.91 2.04 1.48 1.43 1.35 2.18 2.38 2.15 2.77 3.01 2.96 3.06 2.89 2.98 3.04 2.84 2.93 2.71 2.73 3.45 2.52 2.48 2.72 2.38 2.26 1.74 7.48 6.78 2.91 2.37 2.69 3.02

0.32 0.31 0.33 0.33 0.31 0.32 0.32 0.23 0.18 0.21 0.35 0.36 0.33 0.43 0.46 0.47 0.46 0.44 0.48 0.46 0.46 0.47 0.43 0.43 0.54 0.36 0.39 0.39 0.34 0.31 0.26 1.14 1.04 0.45 0.37 0.42 0.45

63

(La/Yb)N EuN/Eu* 5.97 5.25 4.99 4.74 4.98 4.38 5.03 3.79 5.27 4.87 2.87 2.57 2.88 3.39 2.67 2.81 2.44 2.68 2.91 2.67 2.88 2.79 2.75 2.86 2.56 4.01 3.96 3.74 3.95 5.33 3.55 9.97 9.37 2.25 2.84 2.17 2.12

0.97 0.89 0.92 0.87 0.97 0.98 0.87 0.97 0.97 0.89 0.89 0.88 0.92 0.94 0.88 0.92 0.87 0.91 0.91 0.90 0.92 0.91 0.93 0.89 0.96 0.96 0.92 0.94 0.90 1.03 0.98 0.83 0.86 0.82 1.02 0.95 0.98

Table 4. Results of in-situ zircon Hf analyses of the dolerites within the area of the Taihang-Da Hinggan gravity lineament . Hf (t)=10000 {[(176Hf / 177Hf)S – (176Lu/177Hf) S × (et–1)]/ [(176Hf / 177Hf) CHUR,0 – (176Lu / 177Hf) CHUR × (et–1)]–1};TDM1=1/ × in {1+ (176Hf / 177Hf)S – (176Hf/177Hf) DM] / [(176Lu / 177Hf)S – (176Lu / 177Hf) DM]}; TDM2=1/ × in {1+ [(176Hf / 177Hf) S,t – (176Hf / 177Hf)DM, t]/[(176Lu / 177Hf)C – (176Lu / 177Hf)DM]} + t; ƒLu/Hf = (176Lu / 177Hf) S /(176Lu / 177Hf)CHUR-1. The 176Hf / 177Hf and 176Lu / 177Hf ratios of chondrite and depleted mantle at the present are 0.282772 and 0.0332, 0.28325 and 0.0384, respectively (Blichert-Toft and Albare`de 1997; Griffin et al. 2000). =1.867 × 10–11a–1 (Sӧderlund et al. 2004). (176Lu / 177Hf)C = 0.015, t=crystallization age of zircon. Sample LWM01 LWM02 LWM03 LWM06 WJZ01 WJZ03 MJZ03 MJZ04 MJZ05 MJZ11 MJZ18 MJZ25 MJZ28 MJZ36 JY03 JY07 JY14 JY15 HM01 HM03 XHH02 XHH03 XHH04 XHH05

Rb (ppm) 22.3 33.5 17.7 6.02 3.72 3.56 10.4 9.51 14.1 33.4 1.50 1.61 2.43 2.11 6.12 1.91 5.22 4.04 88.8 93.5 22.4 4.32 6.14 3.72

Sr (ppm) 252 242 271 242 196 183 138 133 138 135 146 155 140 133 290 308 295 204 72.8 72.9 135 305 165 146

87Rb/86Sr

0.2561 0.4006 0.1890 0.0720 0.0549 0.0563 0.2189 0.2069 0.2957 0.7160 0.0298 0.0302 0.0504 0.0459 0.0611 0.0179 0.0512 0.0573 3.5300 3.7118 0.4802 0.0410 0.1080 0.0740

87Sr/86Sr

±2s

0.707239 0.707402 0.707064 0.706440 0.706621 0.706621 0.707958 0.707861 0.707928 0.708671 0.707408 0.707623 0.707450 0.707429 0.706588 0.706364 0.706376 0.706407 0.711491 0.711870 0.706049 0.705432 0.705398 0.70527

0.000008 0.000014 0.000007 0.000009 0.000009 0.000009 0.000009 0.000008 0.000013 0.000007 0.000010 0.000008 0.000007 0.000007 0.000007 0.000008 0.000010 0.000006 0.000010 0.000013 0.000007 0.000009 0.000007 0.000006

Sm (ppm) 3.66 3.79 3.72 3.23 2.42 2.24 2.55 2.69 2.54 3.62 3.80 3.73 3.69 3.67 4.49 4.52 4.53 2.38 27.3 23.6 3.51 4.61 3.33 3.71

Nd (ppm) 19.1 17.5 17.9 14.6 10.5 8.48 8.04 8.21 8.52 12.2 12.6 11.7 11.9 12.4 18.0 17.6 19.2 9.33 116.5 107 11.7 17.9 11.4 12.4

147Sm/144Nd

143Nd/144Nd

0.1154 0.1304 0.1251 0.1332 0.1387 0.1590 0.1909 0.1972 0.1795 0.1786 0.1816 0.1919 0.1867 0.1782 0.1502 0.1546 0.1420 0.1536 0.1411 0.1328 0.1806 0.1550 0.1758 0.1801

0.512193 0.512204 0.512215 0.512201 0.512192 0.512182 0.511576 0.511585 0.511589 0.511636 0.511636 0.511623 0.511625 0.511626 0.511829 0.511797 0.511771 0.511816 0.511654 0.511649 0.511616 0.511625 0.511616 0.511653

64

±2s ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### ####### #######

(87Sr/86Sr)i 0.706467 0.706194 0.706494 0.706223

0.706466 0.706461 0.707417 0.707459 0.707355 0.707283 0.707350 0.707564 0.707353 0.707340 0.706469 0.706329 0.706277 0.706296 0.705295 0.705355 0.705207 0.705360 0.705208 0.705140

(143Nd/144Nd)i 0.512033 0.512023 0.512041 0.512016 0.512011 0.512003

εNd (t) -6.5 -6.7 -6.3 -6.8 -7.2 -7.4

0.511458 0.511473 0.511464 0.511512 0.511521 0.511509 0.511508 0.511510

-19.6 -19.3 -19.5 -18.5 -18.4 -18.6 -18.6 -18.6

0.511829 0.511797 0.511771 0.511816 0.511550 0.511541 0.511546 0.511554 0.511544 0.511542

-15.7 -15.7 -16.0 -15.3 -18.1 -18.3 -18.2 -18.0 -18.3 -18.3

Table no 5 Sample

Age (Ma)

206Pb/204Pb

207Pb/204Pb

208Pb/204Pb

U (ppm)

Pb (ppm)

Th (ppm)

(206Pb/204Pb)i

(207Pb/204Pb)i

(208Pb/204Pb)i

LWM01 LWM02 LWM03 LWM06 WJZ01 WJZ03 MJZ03 MJZ04 MJZ05 MJZ11 MJZ18 MJZ25 MJZ28 MJZ36 JY03 JY07 JY14 JY15 HM01 HM03 XHH02 XHH03 XHH04 XHH05

212 212 212 212 199.6 199.6 136.4 136.4 136.4 136.4 136.4 136.4 136.4 136.4 136.4 136.4 136.4 136.4 123.5 123.5 123.3 123.3 123.3 123.3

16.812 16.805 16.861 16.793 16.785 16.794 16.804 16.812 16.883 16.789 16.791 16.791 16.768 16.836 16.766 16.793 16.812 16.865 17.063 17.041 17.048 17.063 17.067 17.061

15.463 15.462 15.458 15.448 15.441 15.443 15.439 15.438 15.443 15.439 15.437 15.439 15.437 15.442 15.436 15.439 15.438 15.443 15.534 15.531 15.534 15.535 15.538 15.536

37.034 37.031 37.033 37.001 37.002 37.004 37.203 37.202 37.194 37.086 37.082 37.061 37.015 37.037 37.014 37.058 37.055 37.159 37.056 37.184 36.993 37.077 37.064 37.086

1.56 1.52 1.54 1.18 1.23 1.24 1.11 1.23 1.95 2.12 2.24 2.16 1.48 1.62 1.43 2.28 2.52 2.31 0.92 0.75 1.21 3.45 3.38 3.66

46.3 21.4 20.8 37.3 36.1 33.2 18.5 18.4 16.2 43.6 45.4 44.3 45.5 18.7 43.6 44.3 37.6 21.8 15.6 19.2 26.2 57.8 55.4 64.6

8.21 4.62 4.58 4.12 4.04 3.92 11.7 11.5 9.75 15.4 15.5 13.2 8.31 4.53 8.14 12.7 10.6 11.5 5.43 13.1 4.78 23.3 20.5 27.2

16.744 16.661 16.711 16.729 16.720 16.723 16.726 16.725 16.726 16.726 16.727 16.728 16.726 16.723 16.723 16.726 16.725 16.727 16.993 16.995 16.994 16.993 16.995 16.994

15.460 15.455 15.450 15.445 15.438 15.439 15.435 15.434 15.435 15.436 15.434 15.436 15.435 15.437 15.434 15.436 15.434 15.436 15.531 15.529 15.531 15.532 15.535 15.533

36.917 36.888 36.887 36.928 36.932 36.931 36.934 36.936 36.937 36.936 36.937 36.934 36.937 36.934 36.935 36.936 36.935 36.934 36.921 36.920 36.923 36.921 36.921 36.923

65

Table 6 LWM01 Spot 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 WJZ03 Spot 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 MJZ02 Spot 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 YJ01 Spot 1 2 3

176Yb/177Hf

0.027346 0.036873 0.048876 0.018427 0.054608 0.036305 0.036916 0.068892 0.023998 0.060865 0.017414 0.046212 0.044853 0.044956 0.017467 0.056231

176Yb/177Hf

0.056223 0.058063 0.042811 0.043577 0.055136 0.036298 0.044768 0.053141 0.054477 0.037234 0.047833 0.045224 0.027634 0.038287 0.040082 0.055065

176Lu/177Hf

0.000793 0.001103 0.001308 0.000554 0.001572 0.001061 0.001040 0.001927 0.000726 0.001697 0.000502 0.001307 0.001340 0.001319 0.000467 0.001475

176Lu/177Hf

0.001564 0.001597 0.001205 0.001298 0.001480 0.000977 0.001284 0.001498 0.001415 0.000992 0.001387 0.001317 0.000771 0.001160 0.001053 0.001477

176Hf/177Hf

0.282007 0.282001 0.282002 0.282008 0.282001 0.282001 0.282003 0.282004 0.282013 0.282013 0.282001 0.282002 0.282005 0.282002 0.282003 0.282002

176Hf/177Hf

0.282022 0.282033 0.282032 0.282022 0.282013 0.282029 0.282011 0.282026 0.282036 0.282039 0.282011 0.282028 0.282020 0.282039 0.282036 0.282035

176Yb/177Hf

176Lu/177Hf

176Hf/177Hf

0.072442 0.056303 0.051207 0.069735 0.023131 0.085032 0.086050 0.035603 0.054731 0.085644 0.034732 0.034649 0.034146 0.054736 0.024197 0.035610 0.034268

0.002053 0.001735 0.001744 0.002062 0.001082 0.002603 0.002622 0.001101 0.001659 0.003186 0.000897 0.001322 0.001076 0.001722 0.001091 0.001104 0.001106

0.282447 0.282441 0.282445 0.282443 0.282410 0.282446 0.282381 0.282437 0.282395 0.282440 0.282436 0.282446 0.282438 0.282396 0.282413 0.282435 0.282437

176Yb/177Hf

176Lu/177Hf

176Hf/177Hf

0.001808 0.001967 0.002210

0.000835 0.000827 0.000731

2s 0.000028 0.000035 0.000020 0.000063 0.000036 0.000026 0.000021 0.000040 0.000041 0.000033 0.000022 0.000029 0.000042 0.000028 0.000020 0.000025

εHf (t) -22.5 -22.8 -22.8 -22.5 -22.8 -22.8 -22.7 -22.8 -22.3 -22.4 -22.7 -22.8 -22.7 -22.8 -22.6 -22.8

TDM1 (Ma) 1744 1766 1775 1731 1788 1764 1761 1801 1732 1777 1738 1775 1772 1775 1734 1783

TDM2 (Ma) 2663 2678 2679 2659 2682 2677 2674 2679 2649 2656 2673 2678 2672 2679 2669 2680

fLu/Hf -0.98 -0.97 -0.96 -0.98 -0.95 -0.97 -0.97 -0.94 -0.98 -0.95 -0.98 -0.96 -0.96 -0.96 -0.99 -0.96

2s 0.000026 0.000028 0.000022 0.000040 0.000026 0.000036 0.000028 0.000034 0.000022 0.000022 0.000024 0.000029 0.000023 0.000024 0.000024 0.000026

εHf (t) -23.9 -23.5 -23.6 -23.9 -24.2 -23.7 -24.3 -23.8 -23.4 -23.3 -24.3 -23.7 -23.9 -23.3 -23.4 -23.5

TDM1 (Ma) 1758 1744 1728 1746 1766 1721 1761 1750 1732 1709 1766 1739 1724 1716 1716 1736

TDM2 (Ma) 2686 2661 2663 2685 2705 2668 2710 2678 2655 2647 2710 2673 2687 2647 2654 2657

fLu/Hf -0.95 -0.95 -0.96 -0.96 -0.96 -0.97 -0.96 -0.95 -0.96 -0.97 -0.96 -0.96 -0.98 -0.97 -0.97 -0.96

εHf (t) -8.7 -8.9 -8.7 -8.8 -9.8 -8.7 -11.0 -8.8 -10.3 -8.8 -8.8 -8.4 -8.7 -10.2 -9.5 -8.7 -8.6

TDM1 (Ma) 1172 1170 1165 1178 1193 1191 1287 1156 1233 1219 1151 1151 1154 1234 1190 1159 1157

TDM2 (Ma) 1738 1749 1740 1745 1812 1741 1885 1751 1846 1754 1749 1731 1746 1842 1801 1750 1746

fLu/Hf -0.94 -0.95 -0.95 -0.94 -0.97 -0.92 -0.92 -0.97 -0.95 -0.90 -0.97 -0.96 -0.97 -0.95 -0.97 -0.97 -0.97

εHf (t) -19.9 -20.2 -20.1

TDM1 (Ma) 1578 1590 1583

TDM2 (Ma) 2441 2461 2456

fLu/Hf -0.97 -0.98 -0.98

2s 0.000019 0.000020 0.000058 0.000019 0.000038 0.000028 0.000023 0.000049 0.000044 0.000061 0.000023 0.000023 0.000027 0.000026 0.000022 0.000051 0.000048

2s 0.000024 0.000019 0.000044

0.282128 0.282119 0.282121 66

4 5 6 7 8 9 10 11 12 13 14 15 16 HM03 Spot 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 XHH01 Spot 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16

0.001890 0.001532 0.004109 0.003520 0.004399 0.004735 0.006154 0.003495 0.002997 0.006720 0.003042 0.005032 0.002082

176Yb/177Hf

0.024835 0.033430 0.042486 0.024181 0.018763 0.013162 0.009441 0.014967 0.028467 0.042885 0.051710 0.026722 0.028310 0.022850 0.033056 0.015541

176Yb/177Hf

0.076671 0.076673 0.056360 0.056345 0.088837 0.048712 0.048703 0.047506 0.130991 0.048118 0.048228 0.047550 0.051707 0.048218 0.047505 0.051696

0.000901 0.000679 0.000724 0.000557 0.000725 0.000648 0.000481 0.000717 0.000810 0.000494 0.000726 0.000731 0.000775

176Lu/177Hf

0.000763 0.001064 0.001254 0.000643 0.000579 0.000364 0.000230 0.000321 0.000834 0.001229 0.001434 0.000802 0.000782 0.000616 0.001046 0.000538

176Lu/177Hf

0.282123 0.282109 0.282143 0.282112 0.282136 0.282149 0.282140 0.282142 0.282130 0.282149 0.282138 0.282170 0.282139

176Hf/177Hf

0.282272 0.282262 0.282265 0.282304 0.282258 0.282304 0.282269 0.282242 0.282277 0.282319 0.282258 0.282256 0.282295 0.282306 0.282259 0.282301

176Hf/177Hf

0.002213 0.282418 0.002215 0.282417 0.001714 0.282453 0.001716 0.282456 0.002564 0.282379 0.001497 0.282345 0.001514 0.282348 0.001798 0.282443 0.003751 0.282409 0.001804 0.282441 0.001790 0.282437 0.001812 0.282429 0.001704 0.282439 0.001785 0.282434 0.001795 0.282445 0.001687 0.282436

67

0.000028 0.000022 0.000036 0.000022 0.000022 0.000030 0.000034 0.000037 0.000059 0.000037 0.000025 0.000032 0.000039

-20.0 -20.5 -19.3 -20.4 -19.6 -19.1 -19.4 -19.4 -19.8 -19.1 -19.5 -18.4 -19.5

1588 1598 1553 1589 1562 1542 1547 1554 1574 1536 1560 1516 1560

2452 2483 2407 2475 2422 2393 2412 2409 2436 2393 2419 2348 2416

-0.97 -0.98 -0.98 -0.98 -0.98 -0.98 -0.99 -0.98 -0.98 -0.99 -0.98 -0.98 -0.98

2s 0.000035 0.000045 0.000050 0.000027 0.000026 0.000020 0.000035 0.000022 0.000031 0.000025 0.000022 0.000050 0.000044 0.000029 0.000044 0.000030

εHf (t) -13.4 -13.8 -13.7 -12.3 -13.9 -12.2 -13.5 -14.4 -13.2 -11.8 -14.0 -14.0 -12.6 -12.2 -13.9 -12.4

TDM1 (Ma) 1376 1401 1403 1327 1389 1317 1361 1401 1371 1327 1420 1399 1345 1324 1404 1327

TDM2 (Ma) 2083 2108 2102 2011 2113 2008 2086 2146 2072 1983 2118 2118 2033 2007 2113 2016

fLu/Hf -0.98 -0.97 -0.96 -0.98 -0.98 -0.99 -0.99 -0.99 -0.97 -0.96 -0.96 -0.98 -0.98 -0.98 -0.97 -0.98

2s 0.000057 0.000061 0.000046 0.000032 0.000033 0.000020 0.000031 0.000031 0.000026 0.000023 0.000039 0.000028 0.000048 0.000024 0.000027 0.000034

εHf (t) -10.0 -10.0 -8.7 -8.6 -11.3 -12.4 -12.3 -8.9 -10.3 -9.0 -9.1 -9.3 -9.0 -9.1 -8.7 -9.0

TDM1 (Ma) 1219 1221 1152 1149 1288 1299 1295 1169 1286 1172 1177 1189 1172 1182 1166 1176

TDM2 (Ma) 1810 1813 1729 1723 1898 1967 1960 1749 1834 1752 1760 1777 1754 1765 1740 1759

fLu/Hf -0.93 -0.93 -0.95 -0.95 -0.92 -0.95 -0.95 -0.95 -0.89 -0.95 -0.95 -0.95 -0.95 -0.95 -0.95 -0.95