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The multiple granitic magmatism in the giant Huayangchuan uranium polymetallic ore district: Implications for tectonic evolution of the southern margin of North China Craton in the Qinling Orogen
Journal Pre-Proof The multiple granitic magmatism in the giant Huayangchuan uranium polymetallic ore district: Implications for tectonic evolution of the southern margin of North China Craton in the Qinling Orogen Chunsi Yang, Liandang Zhao, Hui Zheng, Dequan Wang PII: DOI: Reference:
S0169-1368(19)30164-7 https://doi.org/10.1016/j.oregeorev.2019.103055 OREGEO 103055
To appear in:
Ore Geology Reviews
Received Date: Revised Date: Accepted Date:
22 February 2019 19 June 2019 31 July 2019
Please cite this article as: C. Yang, L. Zhao, H. Zheng, D. Wang, The multiple granitic magmatism in the giant Huayangchuan uranium polymetallic ore district: Implications for tectonic evolution of the southern margin of North China Craton in the Qinling Orogen, Ore Geology Reviews (2019), doi: https://doi.org/10.1016/j.oregeorev. 2019.103055
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The
multiple
granitic
magmatism
in
the
giant
Huayangchuan
uranium
polymetallic
ore
district：
Implications for tectonic evolution of the southern margin of
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North China Craton in the Qinling Orogen
Key Laboratory of Mineralogy and Metallogeny, Guangzhou Institute of Geochemistry, Chinese
Academy of Sciences, Guangzhou 510640, China
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a
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Chunsi Yanga,b, Liandang Zhaoc*, Hui Zhenga,b, Dequan Wangd
University of Chinese Academy of Sciences, Beijing 100049, China
c
School of Earth Science and Resources, Chang’an University, Xi’an 710054, China
d
Sino Shaanxi Nuclear Industry Group, Xi’an 710100, China
*Corresponding
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b
Author: Liandang Zhao
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School of Earth Science and Resources, Chang’an University, No. 126 Yanta Road, Yanta District, Xi’an 710054, China.
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Tel: +86 29 82339059.
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Email address: [email protected]
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Abstract The giant Huayangchuan U–Nb–Pb deposit in the Qinling Orogen is a newly verified carbonatite-hosted deposit in the southern margin of the North China Craton (NCC), central China.
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Granitic magmatism is extensively developed in the Huayangchuan deposit area, but their ages
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and petrogenesis are not well constrained. The exposed granitic rocks are mainly biotite
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monzogranite porphyry, granite pegmatite, granodiorite, and biotite monzogranite with zircon U–
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Pb ages of 1808 ± 10 Ma, 1807 ± 14 Ma, 233 ± 1.4 Ma, and 132 ± 0.6 Ma, respectively. The Paleoproterozoic biotite monzogranite porphyry belongs to shoshonite and metaluminous series,
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showing enrichment of LREE and LILE and depletion of HREE and HFSE, with high Zr + Y
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+ Nb + Ce values and Ga/Al ratios, which are consistent with A-type granite. Whereas, the contemporaneous granite pegmatite dykes with weak mineralization are also cala-alkaline to
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shoshonite and peraluminous series, enriched in Rb, Ba, and LREE, and depleted in Nb, Ta, Ti and HREE. The shoshonite and weakly peraluminous Triassic granodiorite is slightly enriched
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in LREE with flat HREE patterns, enriched in Ba and Sr and depleted in Nb, Ta, P, and Ti, with similar geochemical characteristics to adakite-like rocks. The Early Cretaceous biotite
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monzogranite is characterized by LREE enrichment and flat HREE patterns, belonging to
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shoshonite and metaluminous to weakly peraluminous I-type granite, with U and LILE enrichment, and HFSE-depleted. The high initial 87Sr/86Sr ratios and enriched Nd (εNd(t) = -17.5 to -17.1) and Hf (εHf(t) = -33.2 to -14.6) isotopes reveal that the Huayangchuan granitic rocks are obviously sourced from crustal-derived magmas. Combined with regional geology and this study, we proposed that: (1) the Paleoproterozoic biotite monzogranite porphyry and granite pegmatite were generated from ancient lower crust during post-collisional extension setting; (2) the
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granodiorite was likely sourced from partial melting of thickened lower crust with pelagic
sediments materials addition during the Triassic although the mineralization-related carbonatite having similar age with granodiorite may derive from mantle; and (3) the Early
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Cretaceous biotite monzogranite was mainly sourced from the partial melting of lower crust
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induced by the underplating of the mafic magma. We suggest that the first phase of magma
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occurred in the Huayangchuan district during the Paleoproterozoic following the amalgamation of
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the Eastern and Western blocks along the Trans-North China Orogen. Since the Mesozoic, the ongoing northward subduction of the Yangtze Craton (YZC) resulted in the crust thickening,
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developing the Triassic granitic magmatism and major mineralization associated with carbonatite.
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The widespread Cretaceous granite and deposit in the southern margin of NCC indicate that intracontinental extension and lithospheric thinning occurred in response to the tectonic regime
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transition from NS-trending to EW-trending subduction.
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Keywords: Granitic magmatism; Geochemistry; Sr–Nd–Hf isotopes; Qinling Orogen;
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Huayangchuan U–Nb–Pb deposit
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1. Introduction Granitic rocks are widespread in the continental crust and many granitic rocks are closely associated to mineralization, including pegmatite-hosted rare metal deposits, granite-associated U
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deposits, skarn Fe deposits, and porphyry Cu–Mo deposits (Kemp et al., 2007; Sial et al., 2011;
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Yang et al., 2018). Studies on the geochronology, geochronology, and petrogenesis of granitic
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rocks will offer some important clues not only to their geodynamic settings, but also the metal
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endowment mechanism (Barbarin, 1999; Chen et al., 2017; Sial et al., 2011).
The Qinling Orogen is one of the most important suture zones in the eastern Asia (Dong et al.,
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2013), which has undergone multi-stages of tectono-magmatic thermal events and recorded the
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opening, subduction, and closure of the northernmost Paleo-Tethys from the Early Paleozoic to the Mesozoic (Meng and Zhang, 2000). The southern margin of the North China Craton (NCC),
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located in the northern part of the Qinling Orogen, has undergone complex tectonic evolution and intensive magmatic activity. Dozens of medium to large scale Au deposits (e.g., Tongguan,
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Wenyu, Dongchuang, Yangzhaiyu, and Dahu), U deposit (e.g., Huayangchuan and Taoyuan), and Mo deposit (e.g., Jinduicheng, Huanglongpu, and Jiulong) concentrated in this area, constituting
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the famous Qinling molybdenum metallogenic belt and the second largest Au-producing area in
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China. Several large granitic batholiths such as Laoniushan, Huashan, Wenyu, Niangniangshan, and Heyu and some small granite porphyries like Jinduicheng and Shijiawan developed in this region, with the latter generally thought to be closely related to especially the porphyry Mo mineralization but the former generally barren (e.g., Jinduicheng; Jiao et al., 2010; Zhu et al., 2010). However, recent explorations have identified several medium to large deposits spatially and temporally associated with the large granitic batholiths, e.g., Yuchiling porphyry Mo deposit
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(Li et al., 2009). The Huayangchuan U–Nb–Pb deposit is located in the Huayin County, Shaanxi Province. It was firstly discovered in the early 1970s and detailed exploration began in 2012 by the No. 224
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Brigade, Sino Shaanxi Nuclear Industry Group. It has now been proven to be a world-class
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uranium deposit (detailed resource number is currently confidential). Previous studies generally
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focused on the deposit geology, mineralogy, and geochemistry at Huayangchuan (Gao et al., 2017;
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Guo et al., 2008; He et al., 2016a, b; Hui and He, 2016; Hui et al., 2014; Wang et al., 2011; Wu et al., 2015; Xu, 2009, 2011; Xue et al., 2018; Yu, 1992). Few works has been done on multiphase of
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granitic magmatism, with the relationships between the granitic intrusions and mineralization, and
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tectonic evolution of the Huayangchuan ore district yet not well-documented. Thus, in this contribution, we present newly obtained zircon U–Pb ages and Hf isotope data, whole-rock major
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and trace elements, and whole-rock Sr–Nd isotopes for the granitic intrusions at Huayangchuan. When combined with previous geochemical studies, we will investigate petrogenesis of the
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granitic rocks and discuss the tectonic evolution for the Huayanchuan deposit and the southern
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margin of the NCC.
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2. Regional and deposit geology 2.1 Regional geology The Qinling Orogen, sandwiching between the NCC and the Yangtze Craton (YZC) and
linking the Kunlun Orogen in the west and the Dabie Orogen in the east (Fig. 1a), is a worldrenowned Phanerozoic accretionary orogeny and undergone multi-stages of tectono-magmatic thermal events from the Archaean–Proterozoic to the Mesozoic (Dong et al., 2011; Li et al., 2015;
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Ratschbacher et al., 2003; Wu and Zheng, 2013; Zhang et al., 1995; Zheng et al., 2013). It is bounded by the Sanmenxia-Baofeng Fault to the north and the Longmenshan-Dabashan Fault to the south, and is divided into four major terranes or blocks from north to south, including the
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southern margin of the NCC, the North Qinling Belt, the South Qinling Belt, and the northern
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margin of the YZC, by the Luonan-Luanchuan Fault and the Shangdan and the Mianlue sutures,
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respectively (Fig. 1b). The North Qinling Belt is predominately composed of the Proterozoic
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metasedimentary and metavolcanic rocks. The South Qinling Belt mainly contains Neoarchean– Neoproterozoic volcanic-sedimentary assemblages and overlain by Late Proterozoic to Triassic
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sedimentary sequences. The northern margin of the YZC is characterized by the Neoarchean
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crystalline basement and Mesoproterozoic–Neoproterozoic volcanic and sedimentary sequences, overlain by a thick Sinian to Mesozoic cover sequences (Zhang et al., 1995).
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The southern margin of the NCC, in which the Huayangchuan U–Nb–Pb deposit is located, is bounded by the Sanmenxia-Baofeng Fault to the north and the Luonan-Luanchuan Fault to the
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south, and consists mainly of Archaean (ca. 2.9–2.3Ga) basement and overlain by Proterozoic volcanic and sedimentary sequences (Zhang et al., 1995). The Archaean basement is composed of
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the amphibolite- to granulite-facies metamorphic rocks of the Taihua Group. The Proterozoic
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volcanic and sedimentary sequences comprise the Xiong’er Group, Guandaokou Group, and Luanchuan Group. The Xiong’er Group includes Paleoproterozoic mafic to felsic volcanic rocks with minor sedimentary rocks, whereas the Guandaokou Group consists of Mesoproterozoic quartzite and schist intercalated with dolomitic marble. The Neoproterozoic Luanchuan Group from the basement upwards, includes metasandstone of the Sanchuan Formation, marble and schist of the Nannihu Formation, and dolomitic marble of Meiyaogou Formation (Bao et al., 2014).
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A great amount of Late Paleoproterozoic to Mesoproterozoic intrusions had also developed in the southern margin of the NCC, including mafic dykes swarms (Bi et al., 2011; Wang et al., 2008), syenites and monzonites (Liu, 2011; Ren et al., 2000), and granitic rocks (Deng et al., 2015; Wang
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et al., 2013). Late Paleozoic and Mesozoic granitic intrusions developed widely as large batholiths
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and small porphyries in this region, which were explained as the results of collision and intraplate
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magmatism, respectively (Gao et al., 2014a, b; Mao et al., 2002). The major structures of the
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southern margin of the NCC are characterized by a series of nearly EW-trending faults, which mainly evolved from the Triassic to Jurassic southward thrusting and the Cretaceous northward
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normal faults (Li et al., 2011; Mao et al., 2002; Zhao et al., 2011, 2012). Moreover, the southern
al., 2004; Mao et al., 2008).
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2.2 Deposit geology
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margin of the NCC is an important Mo, Au, Ag, Pb–Zn, W, Sb, and U metallogenic belt (Chen et
The giant Huayangchuan U–Nb–Pb deposit is situated in the western part of the southern
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margin of the NCC (Fig. 1b) and is approximately 8 km to the north of the Huanglongpu Mo ore concentration area. The stratigraphy units in the Huayangchuan district are mainly the
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Sanguanmiao and Qincanggou formations of the Taihua Group and unconsolidated Quaternary
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sediments (Fig. 1c). The Sanguanmiao Formation mainly consists of amphibole–plagioclase gneiss intercalated with plagioclase gneiss, biotite–plagioclase gneiss, granitic gneiss, amphibole gneiss, and migmatite. The Qincanggou Formation is composed of amphibole–plagioclase gneiss intercalated with plagioclase gneiss, biotite–plagioclase gneiss, and granitic gneiss. The main geologic structures of the ore district are nearly NW-trending folds and NW-trending faults. The granitic igneous rocks outcropped in the deposit are mainly the larger plutons (e.g., Laoniushan,
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Huashan, and Xiaohe) and small dykes. The Laoniushan pluton is composed of Late Triassic granitoids, including quartz diorite, biotite monzogranite, quartz monzonite, and hornblende monzonite, and Late Jurassic to Early Cretaceous granitoids, including medium- to coarse-grained
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and medium- to fined-grained biotite monzogranite (Ding et al., 2011; Qi et al., 2012). The
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Huashan pluton consists of Late Triassic hornblende-bearing monzogranite and Early Cretaceous
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monzogranite and biotite monzogranite (Guo et al., 2009; Hu et al., 2012; Zhang et al., 2015). The
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Xiaohe pluton is Paleoproterozoic gneissic granite intercalated with light-color granitic dykes (Fig. 1c; Li, 2011).
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Based on field investigation and previous survey report, the orebodies-hosted carbonatite
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intruded into Archean–Paleoproterozoic metamorphic rocks of the Taihua Group and nearly parallel to the Huayangchuan Fault (Fig. 1c). Except for the carbonatite which hosted the major
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orebodies, the pegmatite dykes also contain minor mineralization at Huayangchuan (Gao et al., 2017). At Huayangchuan, U–Nb mineralization is associated with K-feldspar, actinolite, biotite,
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aegirine-pyroxene, and allanite alterations, whereas Pb mineralization is mainly correlated with
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pyrite, zeolite, and carbonate alterations.
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3. Sample descriptions The fine-grained biotite monzogranite porphyry crops out in the central part of the
Huayangchuan ore district, mainly occurred as NW-trending stocks in the Taihua Group. It has porphyritic texture, with phenocrysts of medium-grained K-feldspar and quartz. It contains quartz (~22 vol%), K-feldspar (~32 vol%), plagioclase(~30 vol%), biotite (~10 vol%), hornblende (~4 vol%), and accessory minerals (~2 vol%) of magnetite, zircon, and apatite (Fig. 2a and b). The
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plagioclase in matrix is partially replaced by sericite (Fig. 2c). The granite pegmatite is widely developed in the ore district and locally associated with the Huayangchuan uranium mineralization. The pale-white granite pegmatite contains quartz (~25
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vol%), K-feldspar (45–48 vol%), plagioclase (15–20 vol%), and minor biotite (5–8 vol%), as well
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as accessory minerals (~2 vol%; Fig. 2d) of zircon, magnetite, and titanite. The coarse-grained K-
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feldspar is subhedral with cross-hatched twinning, and the plagioclase is subhedral and partially
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replaced by sericite (Fig. 2e).
The fine-grained granodiorite is observed in the northern part of ore district. The granodiorite
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is gray, and is composed of fine-grained quartz (~23 vol%), K-feldspar (20–24 vol%), plagioclase
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(40–45 vol%), biotite (4–8 vol%), and hornblende (~2 vol%), with accessory minerals (~2 vol%) of zircon, apatite, magnetite, titanite, and allanite (Fig. 2f). The plagioclase is euhedral to
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subhedral with polysynthetic twinning, whereas the K-feldspar is anhedral with cross-hatched twinning. The biotite was locally altered by chlorite. The hornblende commonly distributed as
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intergranular mineral between the feldspar and quartz (Fig. 2g). The medium- to fine-grained biotite monzogranite crops out in the western part of the ore
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district. The biotite monzogranite is grey white, and contains medium-grained quartz (~22 vol%),
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K-feldspar (30–35% vol%), plagioclase (~30 vol%), and biotite (10–15% vol%), with accessory minerals (~3% vol%) of zircon, apatite, magnetite, and titanite (Fig. 2h). The K-feldspar is mainly subhedral with cross-hatched twinning, and the plagioclase is characterized by polysynthetic twinning and zonation (Fig. 2i).
4. Analytical methods
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4.1 Major and trace elements The whole-rock samples of the Huayangchuan granitic rocks for this study were crushed by jaw crusher and roller mill, and then powdered to less than 200-mesh using agate mortars in order
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to minimize potential contamination of transition metals. Major and trace elements were carried
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out at ALS Chemex (Guangzhou) Co. Ltd. The major element analyses were performed using X-
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ray fluorescence spectrometry (XRF), and the analytical precision is generally better than 2%. The
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trace and rare earth element abundances were determined with a X-series 2 ICP–MS. Precisions are better than 5% for elements in concentrations of more than 10 ppm, and better than 10% for
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elements in concentrations of less than 10 ppm. The detailed analytical procedures are described
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by Liu et al. (2008). The analytical uncertainties for the major elements were < 1%. The analytical accuracy was estimated by the relative difference between the measured and recommended values
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and was < 5% for most elements. 4.2 Sr–Nd isotope analyses
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Samples selected for Sr and Nd isotope analyses were dissolved in Teflon bombs with HF + HNO3 acid solution at 120 °C for 7 days. The solution was dried and re-dissolved in HCl solution
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and then separated by conventional cation-exchange techniques. Sample preparation and chemical
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separation were as described by Liang et al. (2003). Sr–Nd isotope ratios were measured by MC– ICP–MS at the State Key Laboratory of Isotope Geochemistry, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences (GIGCAS). The total procedural blanks were in the range of 200–500 pg for Sr and ≤ 50 pg for Nd. Mass fractionation corrections for Sr and Nd isotope ratios are based on
86Sr/88Sr
= 0.1194 and
146Nd/144Nd
NIST SRM 987 and La Jolla standards yielding measured
= 0.7219, respectively, with the
87Sr/86Sr
and
143Nd/144Nd
ratios of
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0.710265 ± 12 (2σ) and 0.511862 ± 10 (2σ), respectively. 4.3 Zircon U–Pb dating Zircon grains were extracted by conventional heavy liquids and magnetic techniques, and
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then purified by hand picking under binocular microscope. Representative zircon grains were
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mounted in epoxy resin and polished down to expose the grain centre. Zircon U–Pb dating was
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carried out at the Key Laboratory of Mineralogy and Metallogeny, GIGCAS. The isotope and
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trace element compositions of zircon were in-situ measured by laser ablation inductively coupled plasma mass spectrometry (LA–ICP–MS) (Resonetics RESOlution S-155 laser + Agilent 7900)
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with a spot size of 29 μm. This laser ablation system is equipped with a large sample cell (155 mm
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× 105 mm), which can host 20 epoxy sample mounts (with diameter of 25.4 mm). It can wash out 99% signal within less than 1.5 s, because of its two-volume laser-ablation cell. A Squid
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smoothing device was used to reduce statistic error induced by laser-ablation pulses and improve the quality of data (Tu et al., 2011). Helium gas carrying the ablated sample aerosol is mixed with
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argon carrier gas and nitrogen as additional di-atomic gas to enhance sensitivity, and finally flows into ICP. Prior to analysis, the LA–ICP–MS system was optimized using NIST610 ablated with
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29 μm spot size and 5 μm/s scan speed to achieve maximum signal intensity and low oxide rate.
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Each analysis included approximately 20–30 s of back-ground acquisition (from a gas blank) followed by 50 s of data acquisition from the sample. 91500 zircon as the primary standard and Plesovice zircon as the secondary standard to calibrate the U–Pb age of zircon. The reference material (NIST 610) was used as external calibration reference and Si was used as the internal standard to quantify elemental concentrations in samples. The off-line selection and integration of the background and analyte signals, time-drift correction and quantitative calibration, were
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performed using ICPMSDataCal (Liu et al., 2008). 4.4 Zircon Hf isotope analyses All zircon Hf isotope analyses in this study were performed on a Neptune plus MC–ICP–MS
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(Thermo Scientific), coupled with a RESOlution M-50 193 nm laser ablation system (Resonetics),
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which are hosted at the State Key Laboratory of Isotope Geochemistry, GIGCAS. The detailed
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description of the two instruments can be found in Zhang et al. (2014). An X skimmer cone in the
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interface and a small flow of N2 (2 ml/L-1) were used to improve the instrumental sensitivity. All isotope signals are detected with Faraday cups under static mode. The laser parameters were set as
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follow: beam diameter, 45 μm; repetition rate, 6 Hz; energy density, ~4 J/cm-2. Helium was
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chosen as the carrier gas (800 ml/min-1). A “squid” smoothing device on the gas line to the ICP gives a smooth signal. Each analysis consisted of 400 cycles with an integration time of 0.131 s
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per cycle. The first 28 s was used to detect the gas blank with the laser beam off, followed by 30 s laser ablation for sample signals collection with laser beam on. During the measurement of this 180Hf
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study, the gas blank of isobaric interference of
and
176Lu
on
176Hf.
173Yb
175Lu
were used to correct the
The natural ratio values of
The mass bias factor of Yb is calculated from the measured
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and
176Yb/173Yb
and
used in the correction are 0.79381 (Segal et al., 2003) and 0.02656 (Wu et al., 2006).
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176Lu/175Lu
176Yb
was less than 0.2 mv.
173Yb/171Yb
and the natural ratio of
1.13268. The mass bias factor of Lu is assumed to be the same as that of Yb. The mass bias of 176Hf/177Hf
was normalized to
179Hf/177Hf
= 0.7325 with an exponential law. The detailed data
reduction procedure is reported in Zhang et al. (2015). 40 analyses of the Penglai zircon during the course of this study yielded a weighted mean of 176Hf/177Hf = 0.282907 ± 0.000035 (2σ), which is consistent within errors with the reported value in Li et al. (2010).
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5. Results 5.1 Zircon U–Pb geochronology
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LA–ICP–MS zircon U–Pb isotopic results of the fine-grained biotite monzogranite porphyry
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(TLG-14), granite pegmatite (XFG-61), fine-grained granodiorite (HY-01), and medium- to fine-
1
and
illustrated
on
the
concordia
diagrams
(Fig.
3).
The
representative
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Table
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grained biotite monzogranite (HYC-12) from the Huayangchuan ore district are listed in Appendix
cathodoluminescence (CL) images of zircon grains and analyzed spots with U–Pb ages and Lu–Hf
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isotope data are shown in Figure. 4. Zircon grains from all the samples are transparent, and
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euhedral to subeuhedral.
Zircon grains from the biotite monzogranite porphyry are 100 μm to 200 μm long and 50 μm
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to 150 μm wide, with length-to-width ratios of 1:1 to 2:1. They have oscillatory zoning in the CL images (Fig. 4a) and Th/U ratios of 0.85–2.50 (Appendix Tab. 1), suggesting a magmatic origin 206Pb/207Pb
ages ranging from
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(Belousova et al., 2002). Twenty-nine analyzed zircon grains had
1855 Ma to 1737 Ma, yielding a weighted mean 206Pb/207Pb age of 1808 ± 10 Ma (MSWD = 1.1;
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Fig. 3a).
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Zircon grains from the granite pegmatite are generally 150 μm to 300 μm long and 100 μm to
150 μm wide, with length-to-width ratios from 1.2:1 to 3:1. They have clear oscillatory zoning in the CL images (Fig. 4b), with Th/U ratios of 0.26–0.44 (Appendix Tab. 1). Analysis of twentytwo zircon grains had
206Pb/207Pb
ages ranging from 1857 Ma to 1765 Ma, yielding a weighted
mean 206Pb/207Pb age of 1807 ± 14 Ma (MSWD = 1.1; Fig. 3b). Zircon grains from the granodiorite are 200 μm to 300μm long and 50 um to 150 μm wide,
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with length-to-width ratios of 1.5:1 to 4:1. In the CL images (Fig. 4c), these zircons have clear oscillatory zoning with Th/U ratios of 0.24–0.40 (Appendix Tab. 1). All of the analyses plot along a concordia line (Fig. 3c), and two analyzed zircon spots (spot No. 8 and No. 11) had
207Pb/206Pb
age of 238 Ma to 230 Ma, with a weighted mean
age of 233.3 ± 1.4 Ma (MSWD = 1.1; Fig. 3e).
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206Pb/238U
206Pb/238U
age (Fig. 3d).
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Another thirteen grains yielded
206Pb/238U
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concordia line and has not been used to calculate the weighted mean
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ages of 2313 ± 26 Ma and 1835 ± 25 Ma, respectively. One zircon grain deviates from the
Zircon grains from the biotite monzogranite are 100 μm to 300 μm long, 80 μm to 150 μm
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wide with length-to-width ratios of 1:1 to 3:1. The zircon grains have clear oscillatory zoning in
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CL images (Fig. 4d) and Th/U ratios of 0.16–1.39 (Appendix Tab. 1). Twenty-seven analyzed zircons yielded 206Pb/238U ages ranging from 135 Ma to 131 Ma, forming a concordant population
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with a weighted mean 206Pb/238U age of 132.3 ± 0.6 Ma (MSWD = 0.5; Fig. 3f). 5.2 Major and trace elements
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The whole-rock major and trace elements analytical results of the representative granitic rocks samples in the Huayangchuan ore district are shown in Appendix Table 2.
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The fine-grained biotite monzogranite porphyry has SiO2 contents of 60.04–67.87 wt.%,
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Al2O3 contents of 14.35–16.00 wt.%, K2O contents of 4.42–4.60 wt.%, Na2O contents of 4.12– 5.21 wt.%, CaO contents of 1.35–3.29 wt.%, Fe2O3T contents of 4.66–7.74 wt.%, and MgO contents of 0.72–1.48 wt.%, with low Mg# values of 23–28. On the SiO2 vs. Nb/Y diagram (Fig. 5a), most samples plot in alkali granite and monzonite fields. The biotite monzogranite porphyries are shoshonite series (Fig. 5b) and metaluminous (Fig. 5c) with A/CNK values of 0.89–0.97. The biotite monzogranite porphyry is enriched in LREE and depleted in HREE with (La/Yb)N values
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of 46.14–72.24, having negative Eu anomalies (δEu = 0.53–0.71; Fig. 6a). On the primitivenormalized trace element diagram (Fig. 6b), all of the samples show enrichment in the LILE (e.g., Rb, Ba, and Th) and depletion in HFSE (e.g., Nb, Ta, and Ti).
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The granite pegmatite has high SiO2 (72.54–72.93 wt.%), K2O (4.70–6.39 wt.%), Na2O
O
(2.65–3.82 wt.%), and Al2O3 (13.99–14.06 wt.%) contents, and low CaO (0.47–1.12 wt.%), MgO
O
(0.23–0.38 wt.%), and Fe2O3T (1.38–2.39 wt.%) contents, with A/CNK ratios of 0.77–1.11 and
PR
Mg# values of 16–31. They show cala-alkaline and shoshonite affinities, and belong to metaluminous to weakly peraluminous granite (Fig. 5b and c). The granite pegmatite is LREE-
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enriched and HREE-depleted, with (La/Yb)N values of 48.08–268.42, and has variable Eu
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anomalies with δEu values of 0.73–1.52 (Fig. 6c). All the samples are enriched in Rb and Ba, and depleted in Nb, Ta, and Ti (Fig. 6d).
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The fine-grained granodiorite has SiO2 contents of 68.42–74.66 wt.%, K2O contents of 3.96– 4.54 wt.%, plotting in alkali granite field (Fig. 5a) with shoshonite affinity (Fig. 5b). They have
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Al2O3 contents of 13.96–15.43 wt.% and are peraluminous with A/CNK ratios of 1.03–1.04. They also have Na2O contents of 4.96–5.15 wt.%, MgO contents of 0.07–0.16 wt.%, Fe2O3T contents of
U
0.98–1.27 wt.%, and Mg# values of 11–20. The granodiorite is slightly enriched in LREE
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((La/Yb)N = 1.98–11.42), having flat HREE patterns ((Gd/Yb)N = 0.43–0.91) and weakly negative Eu anomalies with δEu values of 0.80–0.91 (Fig. 6e). They are depleted in Nb, Ta, and Ti, and enriched in Ba and Sr (Fig. 6f). The medium- to fine-grained biotite monzogranite has high SiO2 (70.50–71.40 wt.%) and K2O + Na2O contents (8.57–8.77 wt.%), plotting into the alkali granite field (Fig. 5a). They have K2O contents of 4.14–4.43 wt.%, Na2O contents of 4.22–4.37 wt.%, Al2O3 contents of 14.66–
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15.53 wt.%, CaO contents of 1.89–1.99 wt.%, and K2O/Na2O ratios of 0.95–1.04 with A/CNK ratios of 0.97–1.01, plotting in the shoshonite field (Fig. 5b) and belonging to metaluminous to weakly peraluminous granite (Fig. 5c). They have MgO contents of 0.31–0.37 wt.%, Fe2O3T
F
contents of 2.19–2.47 wt.%, and Mg# values of 22–26. All the samples display consistent REE
O
patterns (Fig. 6g), and are characterized by LREE enrichment and flat HREE patterns ((La/Yb)N =
O
24.74–32.07, (Gd/Yb)N = 2.11–2.58; Appendix Tab. 2), having weakly negative Eu anomalies
PR
with δEu values of 0.86–0.92. They are also enriched in U and LILE, and depleted in HFSE (Fig. 6h).
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5.3 Sr–Nd isotopes
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The whole-rock Rb–Sr and Sm–Nd isotope results are listed in Appendix Table 3 and shown in Figure 7a and b. The initial
87Sr/86Sr
isotopic ratios and εNd(t) values for the biotite
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monzogranite porphyry, granite pegmatite, granodiorite, and biotite monzogranite were calculated based on their corresponding zircon U–Pb ages. They have initial
87Sr/86Sr
values of 0.7194–
R N
0.7226, 0.7307–0.7586, 0.7062–0.7177, and 0.7098–0.7100, with corresponding negative εNd(t) values of -7.1 to -6.9, -6.8 to -5.1, -10.5 to -5.9, and -17.5 to -17.1, and two-stage Nd model
U
(TDM2) ages of 2874–2856 Ma, 2845–2701 Ma, 1865–1485 Ma, and 2317–2246 Ma, respectively 87Sr/86Sr
values,
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(Appendix Tab. 3). Comparatively, the granite pegmatite has higher initial
suggesting that it can be easily influenced by later magma activity or alteration events. These granitic rocks are mostly deviated from mantle array and plot in the field of the Taihua Group (Fig. 7a and b), especially in the Neoarchean–Paleoproterozoic Taihua Group evolution domain of the εNd(t)–t evolution diagram (Fig. 7b). 5.4 Zircon Hf isotopes
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Zircon Lu–Hf isotope were determined on the same or similar domains of the zircon grains dated for U–Pb ages in this study. The analytical results are listed in Appendix Table 4 and illustrated in Figure 7c. These zircons yielded 176Hf/177Hf ratios of 0.281400–0.281566, 0.281389–
F
0.281473, 0.281423–0.282388, and 0.281281–0.282280 for the biotite monzogranite porphyry,
O
granite pegmatite, granodiorite, and biotite monzogranite, respectively. Their corresponding εHf(t)
O
values of -8.7 to -8.2, -8.7 to -5.7, -15.4 to -8.5, and -33.2 to -14.6, with two-stage Hf model
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(TDM2) ages of 2977–2636 Ma, 3002–2817 Ma, 2239–1800 Ma, and 3277–2111 Ma, respectively (Appendix Tab. 4). All the analyzed spots plot below the depleted mantle and the chondritic
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E-
uniform reservoir lines, similar to the zircons from the Taihua metamorphic complex (Fig. 7c).
6. Discussion
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6.1 Timing of granitic magmatism
Three pulses of granitic magmatism were identified in the Huayangchuan ore district,
R N
including the Early Proterozoic (ca. 1808 Ma), the Early Mesozoic (ca. 233 Ma), and Late Mesozoic (ca. 132 Ma). Our new LA–ICP–MS zircon U–Pb age of the biotite monzogranite
U
porphyry (1808 ± 10 Ma) is consistent with LA–ICP–MS zircon U–Pb ages of 1803–1797 Ma for
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the Guijiayu monzogranite reported in Deng et al. (2016) and SIMS zircon U–Pb ages of 1829– 1827 Ma for the A-type granite reported by Xue et al. (2018) in the Huayangchuan area. The firstly-reported LA–ICP–MS zircon U–Pb age of 1807 ± 14 Ma for the granite pegmatite in our study broadly distributed in Huayangchuan, further indicates that the Early Proterozoic granitic magmatism was widely developed in the southern margin of the NCC. Based on observations, the spatial relationship between the granite pegmatite dykes and U mineralization could be
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sporadically observed, suggesting that emplacement of the granite pegmatite dykes probably contributed to preliminary enrichment of uranium mineralization at Huayangchuan. Hu et al. (2012) reported a LA–ICP–MS zircon U–Pb age of 205 ± 2 Ma for the Wengyu
F
granite of the Huashan pluton and Qi et al. (2012) gained LA–ICP–MS zircon U–Pb ages of 223 ±
O
1 Ma, 222 ± 1 Ma, and 214 ± 1 Ma for adamellite, granodiorite, and coarse-grained biotite
O
monzogranite of the Laoniushan pluton, respectively. Moreover, mineralization events during the
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Indosinian have been well documented in the southern margin of the NCC, such as the Huanglongpu carbonatite-hosted Mo deposit (ca. 221 Ma; Zhao et al., 2010), the Dashigou
E-
carbonatite-hosted Mo deposit (ca. 216 Ma; Hu, 2013), the Xigou feldspar-quartz vein-hosted Mo
PR
deposit (ca. 212 Ma; Yuan et al., 2014), and the Dahu orogenic lode Au–Mo deposit (ca. 218 Ma; Li et al., 2008). In this study, we obtain a LA–ICP–MS zircon U–Pb age of 233.3 ± 1.4 Ma for the
AL
granodiorite in the Huayangchuan ore district. The giant Huyangchuan U polymetallic deposit is mainly related to carbonatite which shares similar characteristics with the Huanglongpu
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carbonatite-hosted Mo deposit. Integrating the former published regional ages and this study, we propose that the main mineralization period of the Huayangchuan deposit may be formed in the
U
Indosinian.
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Early Cretaceous granites emplaced in the southern margin of the NCC were also
documented, including the Huashan pluton (ca. 146–132 Ma; Hu et al., 2012; Mao et al., 2005; Zhang et al., 2015; Guo et al., 2009), Heyu pluton (ca. 134–127 Ma; Guo et al., 2009; Mao et al., 2005), Laoniushan pluton (ca. 152–146 Ma; Qi et al., 2012; Zhu et al., 2008), Niangniangshan pluton (ca. 142–139 Ma; Gao et al., 2012; Mao et al., 2005), and Wenyu pluton (ca. 138–135 Ma; Gao et al., 2012; Mao et al., 2005). Some Mo mineralization-related granitic magmatism also have
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been reported in the southern margin of the NCC, such as Shijiawan granite porphyry (141 ± 0.6 Ma; Zhao et al., 2010) and Jinduicheng granite porphyry (143.7 ± 3 Ma; Jiao et al., 2010). The biotite monzogranite in the Huayangchuan ore district was formed at 132.3 ± 0.6 Ma, consistent
F
with former reported Late Mesozoic magmatism in this region, although no Mo mineralization
O
was observed in the Huayangchuan biotite monzogranite.
O
6.2 Petrogenesis
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6.2.1 The Paleoproterozoic biotite monzogranite porphyry and granite pegmatite
The fine-grained biotite monzogranite porphyry has relatively high K2O contents of 4.42–
E-
4.58 wt.% (> 4 wt.%), Zr + Nb + Ce + Y contents of 1196–1460 ppm (> 350 ppm), FeOT/(FeOT +
PR
MgO) ratios of 0.81–0.85 (> 0.8), and 10000 Ga/Al ratios of 3.16–3.41 (> 2.6), consistent with Atype granite (Frost et al., 2001; Whalen et al., 1987; Zhang et al., 2012). The presence of
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interstitial Fe-oxide-bearing minerals (e.g., magnetite, hornblende, and biotite; Fig., 2c) also implies an A-type granite character (Bonin, 2007; Landenberger and Collions, 1996). On the Zr vs.
R N
10000 Ga/Al diagram (Fig. 8a), all the samples plot in the A-type granite field, and can be further classified as A1-type granite (Fig. 8b).
U
Various A-type granites worldwide can be attributed to three main petrogenetic scenarios,
JO
including (1) extreme differentiation of mantle-derived tholeiitic or alkaline basaltic magma precursor (Mushkin et al., 2003; Turner et al., 1992); (2) partial melting of crustal rocks (Bonin, 2007; Huang et al., 2011; King et al., 1997; Whalen et al., 1987); and (3) combined crustal and mantle sources, in the form either of crustal assimilation and fractional crystallization (AFC) of mantle-derived magmas, or mixing between mantle-derived and crustal magmas (Kemp et al., 2005; Yang et al., 2006; Zhang et al., 2012). In general, fractional crystallization of a mantle-
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derived magma produces rocks with peralkaline compositions (King et al., 1997; Patiño, 1997; Wu et al., 2002). Obviously, the metaluminous nature of the biotite monzogranite porphyries (Fig. 5c) is inconsistent with the chemical signatures of mantle-derived A-type granite. So the partial
F
melting of crustal rocks and interactions between mantle-derived magma and crustal rocks are
O
likely considered to be the most possible mechanisms for the biotite monzogranite porphyry. The
O
higher calculated zircon saturation temperatures (892–916 °C) may indicate that lower crustal
PR
sources was underplated and heated by mantle-derived mafic magmas to form the biotite monzogranite porphyry. In fact, although coeval ~1.8 Ga mafic dykes have been well documented
E-
in the Xiaoqinling gold district (Bi et al., 2011), the negative εNd(t) and εHf(t) values, in
PR
combination with the absence of mafic enclaves in the pluton and low Mg# values probably favor that the underplating of mafic magma in the lower crustal may have only provided the heat source
AL
for the formation of the biotite monzogranite porphyry. The Neoarchean to Paleoproterozoic basement rocks of the Taihua Group are widespread in
R N
this region. The older two-stage Nd (2874–2856 Ma) and Hf model ages (2977–2636 Ma) of the biotite monzogranite porphyry overlap with the ages of the Taihua Group (ca. 2.9–2.3 Ga; Diwu et 87Sr/86Sr
values of 0.7194–0.7226
U
al., 2018). The biotite monzogranite porphyry has high initial
JO
and negative εNd(t) values of -7.1 to -6.9, which plot in the field of the Taihua Group (Fig. 7a) and follow the trend of Neoarchean–Paleoproterozoic Taihua Group evolution (Fig. 7b). Furthermore, the zircon εHf(t) values of the biotite monzogranite porphyries are plotted in the evolution field of rocks from the Taihua Group (Fig. 7c), also implying that they were most likely derived from partial melting of the basement rocks of the Taihua Group. In summary, the underplating of mafic magmas may have provided heat to induce the partial melting of the Taihua Group and generated
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the Huayangchuan biotite monzogranite porphyry. The granite pegmatite dykes in Huayangchuan ore district have temporal and spatial relationships with the biotite monzogranite porphyry, as well as similar age and geochemical
F
characters, i.e., U–Pb age of 1807 ± 14 Ma, negative εNd(t) and εHf(t) values of -6.79 to -4.99 and
O
-8.7 to -6.7, and the corresponding two-stage Nd and Hf model ages of 2845–2701 Ma and 3002–
O
2817 Ma, which suggest that they may have the same petrogenesis, i.e., partial melting of ancient
6.2.2 The Triassic granodiorite
PR
lower crust.
E-
The fine-grained granodiorite is characterized by weakly negative Eu anomalies (δEu = 0.80–
PR
0.91), with relatively high Sr contents, low Y and Yb contents, and high Sr/Y and (La/Yb)N ratios, which is similar to adakite-like rocks (Fig. 9a; Defant and Drummond, 1990).
AL
Several genetic models have been summarized to account for the origin of adakites and adakitic rocks (Long et al., 2011 and references therein), including (1) partial melting of a
R N
subducting basaltic slab; (2) partial melting of the slab-melt-modified peridotitic mantle wedge; (3) crustal assimilation and fractional crystallization (AFC) processes of parental basaltic magmas; (4)
U
partial melting of delaminated lower crust; and (5) partial melting of thickened lower crust. Based
JO
on the regional and geochemical characteristics of the fine-grained granodiorite, we propose that they were formed by partial melting of thickened lower crust with the following reasons: (1) the Huayangchuan granodiorite is characterized by high SiO2 and K2O contents, low MgO contents and low Mg# values (Appendix Tab. 2), which are different from those of typical slab-derived adakites (Martin et al., 2005); (2) zircons from the granodiorite exhibit strongly negative εHf(t) values, which indicates a significant contribution of old crustal material and preclude an origin
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through partial melting of the slab-melt-modified peridotitic mantle wedge (Martin et al., 2005; Moyen et al., 2001; Stern and Kilian et al., 1996); (3) most adakites formed by crustal assimilation and fractional crystallization (AFC) from coeval parental basaltic magma under high pressure are
F
intermediate and mafic rocks, as basic magmas are unable to directly form high-silicic rocks. This
O
process would generate a large number of mafic rocks in the surrounding area. However, the
O
regional studies indicate that the exposed area of contemporaneous basalt is quite small (Bi et al.,
PR
2011); and (4) some studies indicate that adakitic rocks produced by partial melting of delaminated lower crust should exhibit increased MgO, TiO2, and compatible element abundances
E-
due to metasomatism of mantle peridotite (e.g. Cr, Co, and Ni) and modified Nd–Hf isotopic
PR
systems of the adakitic melts (Castillo, 2006; Chung et al., 2003; Kay and Kay, 1993). Thus, adakitic rocks derived from partial melting of delaminated lower crust are likely to show higher
AL
Mg#, εNd(t), and εHf(t) values than primitive melts of lower crust. However, low MgO and TiO2 contents and compatible element abundances, combined with low Mg#, εNd(t), and εHf(t) values,
R N
suggest that the granodiorite are unlikely to have been derived from partial melting of delaminated lower crust. Two inherent zircons were found from the granodiorite in this study, and have ages of 2313 ± 26 Ma and 1835 ± 25 Ma, respectively. In combination with negative
U
207Pb/206Pb
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εHf(t) values and older two-stage Hf model ages, which may suggest that they were likely generated from the Paleoproterozoic crustal materials and inherited during formation of the Triassic granodiorite. Low contents of Y and HREE in granodiorite rocks indicate that garnet or hornblende may act as residual mineral in magmatic source. Garnet is strongly compatible for HREE and hornblende is relatively compatible for MREE. Hence, when garnet is the main residual mineral in
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magmatic source, the HREE will show strongly fractionated patterns (Y/Yb > 10, (Ho/Yb)N > 1.2; Ge et al., (2002), whereas when hornblende is the main residual mineral in magmatic source, the MREE will show flat patterns (Y/Yb ≈ 10, (Ho/Yb)N ≈ 1.0; Ge et al., 2002). The Huayangchuan
F
granodiorite has Y/Yb and (Ho/Yb)N ratios of 6.69–11.97 and 0.47–1.44, respectively, suggesting
O
that hornblende should be the most important residual mineral and only minor garnet in magmatic
O
source. Previous experimental results suggested that the garnet-in curve was located between 9
PR
Kbar and 14 Kbar in terms of the various compositions of basaltic sources at 800–1000 ℃ (Vielzeuf and Schmidt, 2001). The presence of minor garnet as residual minerals in the
E-
granodiorite source indicates the pressure condition should correspond to the garnet-in curve
PR
nearby, approximately 9–12 Kbar (30–40 km in depth). Noteworthy, the content of Sr in the granodiorite exhibit a widely range of variation, suggesting that a high Sr–Ba magma source, so
AL
the Taihua Group basement rocks cannot to be the single source to produce the Huayangchuan granodiorote. Plank and Langmuir (1998) argued that the variation of Sr should be strongly
R N
attributed to carbonate contribution as a result of that may be influenced by biological productivity and/or hydrothermal processes. Therefore, pelagic sediments material was probably added during
U
the process of the granodiorite magma generation. This view is likely reinforced by the formation
JO
of coeval Dashigou and Yuantou carbonatite-hosted Mo deposit in the Huanglongpu ore field, which derived directly from metasomatized sub-continental lithosphere mantle and exhibited an EM1-type isotopic signature (Song et al., 2015; Xu et al., 2011). As discuss above, we conclude that the granodiorite were derived from partial melting of the ancient basement materials of the Taihua Group and contaminated by pelagic sediments-bearing subducted materials. 6.2.3 The Early Cretaceous biotite monzogranite
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The medium- to fine-grained biotite monzogranite has Na2O contents of 4.22–4.37 wt.% and A/CNK ratios of 0.97–1.01, which are in accordance with the basic feature of I-type granites defined by Chappell and White (1974), i.e., Na2O > 3.2 wt.% and A/CNK < 1.1. However, the
F
biotite monzogranite samples have higher SiO2 (> 70% wt.%) and low P2O5 contents (< 0.11 wt.%;
O
Appendix Tab. 2), and show metaluminous to weakly peraluminous characteristics (Fig. 5c). The
O
Huayangchuan biotite monzogranite is recognized as highly fractionated I-type granites by the
PR
following evidences, including (1) the calculated amounts of corundum in CIPW norm calculations of the biotite monzogranite is absence (C < 1%), which is in accordance with
E-
characteristics of the I-type granites (Chappell and White, 2001); (2) a typical negative correlation
PR
between decreasing Na2O and P2O5 and increasing Si2O (Fig. 10a and b; Chappell, 1999; Green and Watson, 1982; Harrison and Watson, 1984; Li et al., 2007; Watson, 1979; Watson and
AL
Capobianco, 1981; Wolf and London, 1994); and (3) high contents of Th and Y, showing a positive correlation with Rb (Fig. 10c-d; Chappell, 1999; Clemens, 2003; Li et al., 2007).
R N
The biotite monzogranite has relatively high Y/Yb and (Ho/Yb)N ratios of 11.10–11.50 and 1.04–1.18, respectively, suggesting that garnet remained as residual minerals in the source after
U
melt extraction (Ge et al., 2002). Negative Eu anomalies with δEu values of 0.83–0.85 imply
JO
fractional crystallization of plagioclase during the magmatic evolution or plagioclase retention in the magma source. The I-type biotite monzogranite has higher SiO2 contents and relatively lower MgO contents and Mg# values, exhibiting a crustal origin affinity. Zircons of the biotite monzogranite show negative εHf(t) values (-33.2 to -14.6) and relatively older TDM2(Hf) ages (3277–2111 Ma), also suggesting that they were probably derived from ancient lower crust, which is consistent with their negative εNd(t) values of -17.5 to -17.1 and correspondingly old TDM2(Nd)
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ages of 2317–2246 Ma. A role for crustal-derived magmas in the formation of the biotite monzogranite is also suggested by their Y/Yb ratios of 10.94–11.58 (crustal source of Y/Yb > 2; Eby 1992) and Zr/Hf ratios of 34.8-35.2 (crustal source of Zr/Hf > 33; Taylor and Mclennan,
F
1985). However, the biotite monzogranite has Nb/Ta ratios of 16.5-18.8, which suggests an origin
O
of mantle materials (~17.5 for typical primitive mantle; Green, 1995). These evidences may
O
suggest that the biotite monzogranite was formed by melting of ancient lower crust with a minor
PR
contribution of the mantle.
6.3 Implications for geodynamic settings at Huayangchuan and Qinling Orogen
E-
The formation and evolution of the Qinling Orogen has undergone three different stages, i.e.,
PR
(1) Stage I presents the formation of the Neoarchean–Paleoproterozoic and Mesoproterozoic crystalline basement and transitional metamorphic basement; (2) Stage II presents a
AL
Neoproterozoic to Middle Triassic major orogenic period that was controlled by plate tectonics and vertical accretion regimes; and (3) Stage III presents a period of Mesozoic and Cenozoic post-
R N
orogenic intracontinental tectonic evolution (Zhang et al., 1995). Although A-type granites were originally thought to form in rift zones or stable continental
U
blocks (Loiselle and Wones, 1979), they can also form in both anorogenic and post-orogenic
JO
settings (Bonin, 1990; Eby, 1992; Pitcher, 1997; Sylvester, 1989; Whalen et al., 1987). On the tectonic discrimination diagrams of Rb vs. (Y+Nb) and R2 vs. R1, all the samples plot in the fields of post-collisional granites (Fig. 11a) and late orogenic granites (Fig. 11b). In addition, the biotite monzogranite porphyries exhibit high-K calc-alkaline affinity, which is consistent with the granites that formed in the orogenic belts associated with the late stage of continental collision (Barbarin, 1999). The fine-grained biotite monzogranite porphyry at Huayangchuan yields a U–Pb
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age of 1808 Ma, which is slightly later than the amalgamation of the eastern and western blocks of the NCC along the Trans-North China Orogen at ca. 1.85 Ga (Liu et al., 2009; Song et al., 1996; Zhao, 2001; Zhai et al., 2005). During this period, granitic rocks with ages of ca. 1.8 Ga were
F
widely distributed in the NCC (Deng et al., 2016; Gao et al., 2013; Geng et al., 2004, 2006; Liu et
O
al., 2014; Wang et al., 2010; Xue et al., 2018; Zhao and Zhou, 2009; Zhao et al., 2008) and mafic
O
dykes and volcanic rocks of similar ages also have been recognized in the southern margin of the
PR
NCC (Bi et al., 2011; Wang et al., 2008; Zhao et al., 2004), which generally show no evidence of deformation and metamorphism and consistent with anorogenic or post-orogenic magmatism.
E-
Alternatively, they may be linked to extensional setting after the amalgamation of the NCC along
PR
the Trans-North China Orogen. The coeval granite pegmatite at Huayangchuan has a consistent spatial and temporal correlation with the biotite monzogranite porphyry, suggesting that they were
AL
likely emplaced in the same tectonic setting. The upwelling of asthenosphere resulted in partial melting of lower crust could be triggered by underplating of mantle-derived magma or
R N
lithospheric delamination (Fan et al., 2001; Lu et al., 2006; Muir et al., 1995; Petford and Atherton, 1996; Zhang et al., 2002). The granitic porphyry has MgO and Mg# values of 0.72–1.48 wt.% and
U
23–29, respectively, which is inconsistent with the magma formed by lithospheric delamination.
JO
Therefore, we draw a conclusion that underplating of mantle-derived magma induced partial melting of the Taihua Group and formed the biotite monzogranite porphyry and granite pegmatite. During the Late Triassic to Early Cretaceous, the NCC and the YZC collided and resulted in
the formation of the Qinling Orogen (Chen, 2010; Dong et al., 2012 and references therein). In the Triassic, the eastern part of the Qinling Orogen underwent deep continental subduction when the YZC subducted beneath the NCC (Zhu et al., 2011), and the Qinling Paleo-Tethys finally closed
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in a westward zipper-like way at ca. 230–200 Ma (Chen, 2010). In this study, we obtained a U–Pb age of 233 Ma for the granodiorite at Huayangchuan, which is corresponding to Mesozoic and Cenozoic post-orogenic intracontinental tectonic evolution of the Qinling Orogen (Fig. 11a and b).
F
They have identical crystallization ages with Late Triassic granites in the South Qinling (Gong et
O
al., 2009a, b; Qin et al., 2009, 2010; Sun et al., 2002), North Qinling (Lu et al., 1996; Gong et al.,
O
2009a; Zhang et al., 2009), and West Qinling (Zhang et al., 2006, 2007), and mineralization in the
PR
southern of the NCC (Li et al., 2008; Zhao et al., 2010; Zhu et al., 2011; Hu, 2013; Yuan et al., 2014). Meanwhile, the metamorphic ages of ca. 242–221 Ma for the Mianlue ophiolite (Li et al.,
E-
1996) and ca. 240–216 Ma for the Mianlue blueschist (Mattauer et al., 1985; Yin et al., 1991) in
PR
the East Qinling are consistent with the metamorphic ages of 240 Ma to 225 Ma for the UHP metamorphic rocks in the Dabie-Sulu orogenic belt (Zheng et al., 2009). Accordingly, we argued
AL
that the granodiorite at Huayangchuan was likely formed in a post-collisional setting. In this period, the lithosphere was strongly compressed and thickened, inducing to the partial melting of
R N
lower crust to form the granodiorite.
Since Late Mesozoic, the Qinling Orogen was spatially located in the conjugation site of the
U
India, Eurasian, and Pacific plates, and significantly influenced by the Pacific Plate. At ca. 145 Ma,
JO
the Qinling Orogen underwent a tectonic transition in subduction direction from NS-trending to EW-trending (Lu, 1998; Ren, 1991; Zhao et al., 1994), which resulted in the large-scale Late Mesozoic magmatism and mineralization throughout the Qinling Orogen caused by lithospheric extension and thinning. The biotite monzogranite in the Huayangchuan ore district has a U–Pb age of 132 Ma, which is slightly younger than peak ages of tectonic regime transition. Based on this study and the available geological data, the Qinling region has evolved into an intracontinental
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extensional setting during the Early Cretaceous. Hence, we can conclude that the biotite monzogranite was likely emplaced in an extension setting, resulting from partial melting of the lower crust induced by the underplating of the mafic magmas, with minor addition of mantle
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material.
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7. Conclusions
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(1) Three pules of magmatism were identified in the Huayangchuan uranium polymetallic deposit: ca. 1.8 Ga fine-grained biotite monzogranite porphyry and granite pegmatite, ca. 233 Ma
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fine-grained granodiorite, and ca. 132 Ma medium- to fine-grained biotite monzogranite.
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(2) The biotite monzogranite porphyries (ca. 1808 Ma) and granite pegmatite (ca. 1807 Ma) have enriched Nd and Hf isotopes (εNd(t) <0; εHf(t) <0) and old two-stage Nd (2874–2856 Ma) and
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Hf model ages (2977–2636 Ma), indicating that they were generated from ancient lower crust during post-collision extension setting.
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(3) The granodiorites are similar to adakite-like rocks, and have high Sr and Ba contents and negative εNd(t) and εHf(t) values, suggesting that they were derived from partial melting of the
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thickened ancient crust of the Taihua Group and contaminated pelagic sediments-bearing
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materials.
(4) The biotite monzogranites belong to I-type granites and were probably sourced from the
partial melting of lower crust induced by the underplating of the mafic magmas during an extension setting in response to tectonic regime transition from NS-trending to EW-trending.
Acknowledgements
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This study was funded by the joint research project of Guangzhou Institute of Geochemistry, Chinese Academy of Sciences and Sino Shaanxi Nuclear Industry Group (No. Y631141001). We are grateful to the No. 224 Brigade Co. Ltd., Sino Shaanxi Nuclear Industry Group for assistance
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in field work. We thank Dr. Dan Wu and Dr. Le Zhang for zircon U–Pb dating and Sr–Nd–Hf
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isotope analyses, respectively. Comments from two anonymous reviewers are also very helpful to
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us to better present our results and discussion in this manuscript.
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Constraints on the geodynamic setting for the newly discovered Wenquan Mo deposit. Ore Geol. Rev. 39, 46–62. Zindler, A., Hart, S.R., 1986. Chemical geodynamics. Ann. Rev. Earth Planet. Sci. Lett. 14, 493–
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Figure captions
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Fig. 1. (a) The tectonic map of China, showing the location of the Qinling Orogen (after Chen et al., 2009). (b) Tectonic subdivision of the Qinling Orogen (after Zhang et al., 2007). (c) Simplified
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geological map of the Huayangchuan deposit (after Gao et al., 2017).
Fig. 2. Hand specimen photograph and representative photomicrograph of the granitic rocks in the
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Huayangchuan ore district. (a–c) Biotite monzogranite porphyry. (d–e) Granite pegmatite. (f–g) Granodiorite. (h–i) Biotite monzogranite. Abbreviations: Bt: biotite, Hbl: hornblende, Kfs: K-
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feldspar, Mt: magnetite, Pl: plagioclase, Q: quartz.
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Fig. 3. Zircon U–Pb concordia diagrams for granitic rocks in the Huayangchuan ore district.
Fig. 4. The representative zircon CL images for granitic rocks in the Huayangchuan ore district.
Fig. 5. Major and trace element diagram for the granitic rocks in the Huayangchuan ore district. (a) SiO2 vs. Nb/Y diagram (after Maniar and Piccoli, 1994). (b) Th/Yb vs. Ta/Yb diagram (after Muller, 1992). (c) A/NK vs. A/CNK diagram (after Maniar and Piccoli, 1989).
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Fig. 6. Chondrite-normalized REE distribution patterns and primitive-mantle normalized trace element variation diagrams for the granitic rocks in the Huayangchuan ore district. Normalized
87Sr/86Sr
diagram (a, after Zindler and Hart, 1986), εNd(t) vs. time (Ma)
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Fig. 7. εNd(t) vs. initial
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values are from Sun and Mcdonough (1989).
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diagram (b, after Zhao et al., 2012), and εHf(t) vs. age diagram (c, after Hu et al., 2012) for the granitic rocks. εNd(t) and εHf(t) fields of the Taihua Group are from Zhao et al. (2012) and
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references therein and Deng et al. (2016), respectively.
Fig. 8. (a) Zr vs. 10000Ga/Al discrimination diagram for the granitic rocks in the Huayangchuan
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ore district (after Whalen et al., 1987). (b) Distinguishing diagram between A1 and A2 type
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granites (after Eby, 1992).
Fig. 9. (La/Yb)N vs. YbN diagram (a, after Defant and Drummond, 1990) and La/Sm vs. La
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diagram (b, after Allègre and Minster, 1978) for the granitic rocks in the Huayangchuan ore
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district.
Fig. 10. Chemical variation diagrams for the granitic rocks in the Huyangchuan ore district. (a) Na2O vs. SiO2 (after Chappell and White, 1992). (b) P2O5 vs. SiO2 (after Chappell and White, 1992). (c) Th vs. Rb (after Chappell, 1999). (d) Y vs. Rb (after Chappell, 1999).
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Fig. 11. Diagrams of tectonic discrimination for the granitic rocks in the Huyangchuan ore district. (a) Rb vs. (Y+Nb) (after Pearce et al., 1984); (b) R2 vs. R1 (after Batchelor and Bowden, 1985). Abbreviations: syn-COLG = syn-collisional granites; VGA = volcanic-arc granites; ORG = ocean-
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ridge granites; WPG = within-plate granites; Post-COLG = post-collisional granites. Tectonic
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areas from Fig. 11b with numbers are representing mantle fractions, pre-plate collision, post-
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– 11(Na + K) – 2(Fe + Ti); and R2 = 6Ca + 2Mg + Al.
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collision uplift, late-orogenic, anorogenic, syn-collision and post-orogenic, respectively. R1 = 4Si
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Table captions
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Huayangchuan ore district.
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Table 1. LA–ICP–MS zircon U–Pb isotopic compositions of granitic rocks in the giant
Table 2. Major (wt.%), trace, and earth element (ppm) compositions of granitic rocks in the giant
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Huayangchuan ore district.
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Table 3. Whole-rocks Rb–Sr and Sm–Nd isotopic compositions of granitic rocks in the giant
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Huayangchuan ore district.
Table 4. Zircon Lu–Hf isotopic compositions of granitic rocks in the giant Huayangchuan ore district.
JO
U
R N
AL
PR
E-
PR
O
O
F
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JO
U
R N
AL
PR
E-
PR
O
O
F
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JO
U
R N
AL
PR
E-
PR
O
O
F
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JO
U
R N
AL
PR
E-
PR
O
O
F
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JO
U
R N
AL
PR
E-
PR
O
O
F
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JO
U
R N
AL
PR
E-
PR
O
O
F
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U
R N
AL
PR
E-
PR
O
O
F
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O
F
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TLG-14
Pb
Th
U
Th/U
Biotite monzogranite porphyry 223
191
1.16
TLG-14-02
120
265
206
1.28
TLG-14-03
87.0
179
166
1.08
TLG-14-04
114
213
TLG-14-05
108
191
TLG-14-06
133
380
TLG-14-07
115
239
TLG-14-08
219
TLG-14-09
1σ
206Pb/238U
1σ
207Pb/206Pb
0.1132
0.0018
5.0846
0.0950
0.3238
0.0041
1851
0.1130
0.0018
5.2796
0.0941
0.3364
0.0037
1850
0.1111
0.0017
5.0227
0.0891
0.3257
0.0037
1818
203
1.05
0.1134
0.0016
5.3574
0.0901
0.3397
0.0033
1855
225
0.85
0.1106
0.0016
4.8616
0.0731
0.3172
0.0034
1810
189
2.02
0.1097
0.0017
5.0289
0.0858
0.3302
0.0036
1794
213
1.12
0.1084
0.0017
5.1021
0.0883
0.3391
0.0039
1773
620
338
1.84
0.1063
0.0017
4.7539
0.0812
0.3221
0.0034
1737
121
279
213
1.31
0.1075
0.0018
4.9074
0.0880
0.3287
0.0035
1767
TLG-14-10
237
623
389
1.60
0.1079
0.0016
4.8514
0.0783
0.3237
0.0033
1765
TLG-14-11
159
461
221
2.09
0.1077
0.0016
4.9557
0.0820
0.3313
0.0034
1761
TLG-14-12
89.7
192
162
1.19
0.1124
0.0019
5.1670
0.0962
0.3309
0.0034
1839
TLG-14-13
114
266
188
1.42
0.1094
0.0015
5.1630
0.0860
0.3399
0.0040
1791
TLG-14-14
123
272
212
1.28
0.1087
0.0016
5.0750
0.0810
0.3366
0.0037
1789
TLG-14-15
68.8
158
120
1.31
0.1110
0.0018
5.1196
0.0915
0.3320
0.0033
1817
TLG-14-16
215
524
343
1.53
0.1085
0.0015
5.0356
0.0786
0.3341
0.0033
1776
TLG-14-17
131
291
231
1.26
0.1114
0.0018
5.1246
0.0892
0.3312
0.0036
1833
TLG-14-18
114
270
185
1.45
0.1114
0.0017
5.2492
0.0946
0.3389
0.0039
1833
TLG-14-19
161
400
285
1.40
0.1098
0.0016
4.8391
0.0787
0.3168
0.0030
1796
TLG-14-20
211
581
304
1.91
0.1109
0.0015
5.1376
0.0816
0.3332
0.0036
1815
TLG-14-21
272
843
338
2.50
0.1103
0.0015
5.1154
0.0750
0.3335
0.0031
1806
TLG-14-22
99.3
233
162
1.44
0.1123
0.0018
5.2438
0.0886
0.3362
0.0038
1839
TLG-14-23
161
444
244
1.82
0.1111
0.0017
5.0568
0.0827
0.3277
0.0035
1817
TLG-14-26
73.8
155
131
1.19
0.1104
0.0019
5.3323
0.1015
0.3478
0.0047
1806
TLG-14-27
63.2
151
108
1.40
0.1123
0.0020
5.2610
0.1064
0.3378
0.0047
1839
TLG-14-28
75.2
172
130
1.32
0.1115
0.0018
5.1955
0.0878
0.3360
0.0034
1833
TLG-14-30
185
535
256
2.09
0.1105
0.0016
5.1034
0.0774
0.3330
0.0032
1809
JO
R N
AL
PR
102
1σ
207Pb/235U
U
TLG-14-01
Isotope ratio
207Pb/206Pb
E-
Element(ug/g)
Spot
PR
Table 1. LA–ICP–MS zircon U–Pb isotopic compositions of granitic rocks in the giant Huayangchuan ore district.
JOURNAL PRE-PROOF Element(ug/g)
Spot
Th/U
Isotope ratio 207Pb/206Pb
Pb
Th
U
TLG-14-31
163
389
287
1.35
0.1111
0.0016
TLG-14-32
119
261
213
1.23
0.1106
0.0017
XFG-61
1σ
207Pb/235U
1σ
206Pb/238U
1σ
207Pb/206Pb
4.9862
0.0768
0.3236
0.0032
1818
5.1061
0.0836
0.3328
0.0034
1810
Granite pegmatite 386
304
997
0.30
0.1132
0.0020
5.3288
0.0976
0.3378
0.0034
1851
XFG-61-02
134
107
358
0.30
0.1124
0.0019
5.1495
0.0969
0.3289
0.0040
1839
XFG-61-03
448
459
1128
0.41
0.1135
0.0017
5.2427
0.0880
0.3316
0.0037
1857
XFG-61-04
488
476
1245
0.38
0.1135
0.0016
5.1872
0.0838
0.3280
0.0033
1855
XFG-61-05
240
193
618
0.31
0.1135
0.0016
5.2579
0.0832
0.3327
0.0033
1857
XFG-61-10
373
293
970
0.30
0.1120
0.0019
5.2078
0.0952
0.3348
0.0038
1831
XFG-61-11
271
221
692
0.32
0.1122
0.0018
5.2644
0.0952
0.3373
0.0036
1836
XFG-61-12
332
254
852
0.30
0.1108
0.0017
5.1903
0.0825
0.3371
0.0030
1813
XFG-61-13
462
453
1129
0.40
0.1097
0.0015
5.2097
0.0788
0.3419
0.0031
1794
XFG-61-14
292
306
731
0.42
0.1097
0.0016
5.0396
0.0833
0.3308
0.0035
1794
XFG-61-15
319
343
789
0.44
0.1094
0.0016
4.9650
0.0848
0.3266
0.0035
1791
XFG-61-16
335
243
871
0.28
0.1087
0.0016
5.0727
0.0894
0.3359
0.0037
1789
XFG-61-17
369
284
966
0.29
0.1081
0.0019
4.9911
0.0971
0.3327
0.0038
1769
XFG-61-18
449
392
1124
0.35
0.1083
0.0017
5.0123
0.0858
0.3339
0.0032
1770
XFG-61-19
323
235
857
0.27
0.1088
0.0016
4.9913
0.0842
0.3310
0.0033
1789
XFG-61-20
281
191
XFG-61-21
281
242
XFG-61-22
351
275
XFG-61-25
232
203
XFG-61-26
371
XFG-61-27 XFG-61-28
O
O
PR
PR
E-
0.26
0.1088
0.0016
5.0254
0.0867
0.3332
0.0033
1789
695
0.35
0.1079
0.0016
5.0121
0.0801
0.3358
0.0031
1765
900
0.31
0.1075
0.0016
4.9362
0.0826
0.3318
0.0031
1767
602
0.34
0.1087
0.0020
4.8780
0.1057
0.3244
0.0041
1789
329
934
0.35
0.1087
0.0019
4.8931
0.0975
0.3252
0.0038
1789
224
171
561
0.31
0.1096
0.0018
5.0675
0.0891
0.3342
0.0029
1794
406
380
973
0.39
0.1100
0.0017
5.2061
0.0905
0.3417
0.0034
1799
AL
740
Granodiorite 133
904
3347
0.27
0.0510
0.0009
0.2656
0.0048
0.0376
0.0004
242.7
HY-01-03
177
1485
4379
0.34
0.0523
0.0008
0.2718
0.0053
0.0374
0.0005
298.2
HY-01-07
191
1266
4831
0.26
0.0553
0.0013
0.2888
0.0092
0.0370
0.0005
433.4
HY-01-08
321
458
522
0.88
0.1471
0.0023
8.1881
0.1425
0.4005
0.0043
2313
HY-01-10
113
752
2867
0.26
0.0519
0.0010
0.2658
0.0053
0.0369
0.0005
283.4
HY-01-11
315
912
449
2.03
0.1121
0.0016
5.0136
0.0810
0.3221
0.0035
1835
HY-01-13
146
1215
3657
0.33
0.0518
0.0008
0.2678
0.0051
0.0373
0.0005
276.0
HY-01-14
103
663
2639
0.25
0.0555
0.0014
0.2877
0.0086
0.0370
0.0004
435.2
HY-01-18
127
1002
3333
0.30
0.0510
0.0008
0.2583
0.0045
0.0365
0.0004
239.0
HY-01-21
132
958
3301
0.29
0.0562
0.0010
0.2818
0.0044
0.0364
0.0003
461.2
HY-01-22
198
1834
4532
0.40
0.0654
0.0013
0.3396
0.0081
0.0371
0.0003
787.0
HY-01-25
137
1063
3490
0.30
0.0492
0.0009
0.2516
0.0050
0.0368
0.0004
166.8
HY-01-28
114
835
3048
0.27
0.0516
0.0009
0.2615
0.0058
0.0363
0.0005
333.4
HY-01-30
118
742
3066
0.24
0.0538
0.0014
0.2782
0.0080
0.0370
0.0004
364.9
HY-01-31
97.5
600
2460
0.24
0.0551
0.0015
0.2878
0.0088
0.0374
0.0004
416.7
HY-01-32
106
684
2712
0.25
0.0542
0.0011
0.2724
0.0049
0.0364
0.0004
376.0
JO
HY-01-01
U
R N
HY-01
F
XFG-61-01
JOURNAL PRE-PROOF Element(ug/g)
Spot HYC-12
Pb
Th
U
Isotope ratio
Th/U
207Pb/206Pb
1σ
207Pb/235U
1σ
206Pb/238U
1σ
207Pb/206Pb
Biotite monzonitic granite 21.7
637
699
0.91
0.0484
0.0017
0.1394
0.0050
0.0209
0.0003
120.5
HYC-12-02
21.4
353
920
0.38
0.0484
0.0017
0.1376
0.0050
0.0207
0.0003
116.8
HYC-12-03
8.70
237
326
0.73
0.0469
0.0026
0.1322
0.0072
0.0208
0.0004
42.7
HYC-12-04
17.0
301
699
0.43
0.0498
0.0018
0.1427
0.0051
0.0208
0.0002
183.4
HYC-12-05
11.0
279
426
0.65
0.0505
0.0024
0.1464
0.0077
0.0211
0.0004
216.7
HYC-12-06
10.6
234
439
0.53
0.0495
0.0026
0.1400
0.0072
0.0207
0.0004
172.3
HYC-12-07
17.3
208
781
0.27
0.0489
0.0016
0.1428
0.0055
0.0211
0.0004
142.7
HYC-12-08
8.25
287
230
1.25
0.0487
0.0030
0.1372
0.0077
0.0208
0.0004
200.1
HYC-12-09
10.6
181
418
0.43
0.0496
0.0023
0.1410
0.0066
0.0209
0.0004
172.3
HYC-12-10
21.7
199
988
0.20
0.0513
0.0017
0.1464
0.0050
0.0207
0.0002
253.8
HYC-12-11
12.5
95.9
587
0.16
0.0503
0.0018
0.1465
0.0057
0.0211
0.0004
209.3
HYC-12-12
66.7
1258
2462
0.51
0.0501
0.0012
0.1465
0.0035
0.0211
0.0002
198.2
HYC-12-13
23.3
280
1091
0.26
0.0507
0.0015
0.1428
0.0043
0.0205
0.0003
227.8
HYC-12-14
19.7
218
927
0.24
0.0491
0.0016
0.1394
0.0047
0.0206
0.0002
150.1
HYC-12-15
22.6
873
626
1.39
0.0500
0.0020
0.1413
0.0056
0.0205
0.0003
198.2
HYC-12-16
29.4
539
1225
0.44
0.0503
0.0016
0.1450
0.0049
0.0209
0.0003
209.3
HYC-12-17
40.8
865
1644
0.53
0.0483
0.0013
0.1371
0.0039
0.0205
0.0002
122.3
HYC-12-18
24.1
279
1100
0.25
0.0493
0.0015
0.1404
0.0044
0.0206
0.0002
161.2
HYC-12-19
14.6
117
691
0.17
0.0508
0.0016
0.1469
0.0047
0.0208
0.0002
235.3
HYC-12-20
40.1
551
1761
0.31
0.0492
0.0011
0.1418
0.0036
0.0207
0.0003
153.8
HYC-12-21
21.8
174
1038
0.17
0.0464
0.0012
0.1324
0.0035
0.0206
0.0002
16.8
HYC-12-22
27.5
551
1115
0.49
0.0483
0.0013
0.1393
0.0041
0.0208
0.0003
122.3
HYC-12-23
18.6
219
826
0.26
0.0482
0.0015
0.1391
0.0045
0.0209
0.0003
109.4
HYC-12-24
24.2
306
1091
0.28
0.0493
0.0014
0.1392
0.0040
0.0205
0.0002
161.2
HYC-12-25
15.1
118
738
0.16
0.0499
0.0016
0.1441
0.0051
0.0209
0.0003
187.1
HYC-12-26
16.9
552
531
1.04
0.0495
0.0020
0.1404
0.0054
0.0207
0.0002
172.3
HYC-12-27
7.34
67.5
345
0.20
0.0505
0.0022
0.1438
0.0063
0.0207
0.0003
216.7
O
O
PR
E-
PR
AL
U
R N
F
HYC-12-01
JO
Table 2. Major (wt.%), trace and earth element (ppm) compositions of granitic rocks in the giant Huayangchuan ore district. NO.
TLG-14
TLG-15
TLG-16
XFG-61
Biotite monzogranite porphyry
LJG-03
LJG-04
HY-01
Grante pegmatite
HY-02
HY-03
Granodiorite
SiO2
61.19
60.04
67.87
72.54
72.66
72.93
73.51
68.42
74.66
TiO2
0.93
0.99
0.57
0.15
0.11
0.11
0.05
0.06
0.03
Al2O3
15.61
16.00
14.35
14.06
13.99
14.07
14.35
15.43
13.96
TFe2O3
6.70
7.74
4.66
2.39
1.38
2.37
0.98
1.27
1.13
MnO
0.08
0.09
0.10
0.05
0.04
0.05
0.04
0.04
0.06
MgO
1.37
1.48
0.72
0.38
0.31
0.23
0.07
0.16
0.07
CaO
3.29
2.44
1.35
0.47
1.12
1.00
0.43
0.18
0.41
JOURNAL PRE-PROOF
NO.
TLG-14
TLG-15
TLG-16
XFG-61
Biotite monzogranite porphyry
LJG-03
LJG-04
HY-01
Grante pegmatite
HY-02
HY-03
Granodiorite
4.12
5.21
4.49
3.82
2.65
3.69
4.96
1.66
5.15
K2O
4.42
4.60
4.58
5.06
6.39
4.70
4.54
10.85
3.96
P2O5
0.29
0.33
0.15
0.05
0.03
0.02
0.01
0.01
0.01
LOI
0.91
0.44
0.34
0.58
0.60
0.91
0.37
0.48
0.40
Total
98.91
99.36
99.18
99.55
99.28
100.08
99.31
98.56
99.84
K2O+Na2O
8.54
9.81
9.07
8.88
9.04
8.39
9.50
12.51
9.11
K2O/Na2O
1.07
0.88
1.02
1.32
2.41
1.27
A/CNK
0.89
0.89
0.97
1.11
1.05
1.08
A/NK
1.35
1.18
1.16
1.19
1.24
A.R.
2.65
3.27
3.74
4.14
3.98
R1
1387
854
1724
2227
R2
726
648
462
Mg#
29
27
23
La
148
162
248
Ce
301
325
459
Pr
32.4
34.5
44.5
Nd
107
113
Sm
15.8
15.8
Eu
2.85
2.86
2.34
Gd
9.85
9.65
Tb
1.19
1.17
Dy
5.73
Ho
0.77
1.03
1.04
1.03
1.26
1.10
1.06
1.09
3.51
4.60
9.07
4.46
2366
2385
2047
1398
2188
345
410
394
PR
331
330
321
24
31
16
12
20
11
33.4
71.5
87.1
11.4
12.0
3.80
82.2
126
198
20.2
24.9
7.20
6.26
11.2
17.6
1.93
3.42
0.76
134
20.5
30.7
52.9
6.60
14.7
2.80
17.7
2.89
2.99
6.61
1.23
3.53
0.61
0.65
0.98
1.08
0.33
0.93
0.17
10.3
1.76
1.30
3.10
0.99
2.95
0.69
1.23
0.19
0.11
0.31
0.15
0.38
0.12
5.48
6.25
1.04
0.47
1.25
0.89
1.85
0.80
0.98
1.00
1.10
0.19
0.08
0.20
0.20
0.35
0.21
2.54
2.51
2.83
0.47
0.19
0.51
0.70
0.83
0.73
0.36
0.36
0.42
0.07
0.03
0.07
0.12
0.12
0.16
2.16
2.13
2.32
0.47
0.18
0.42
0.88
0.71
1.30
Lu
0.35
0.34
0.36
0.09
0.03
0.07
0.15
0.10
0.25
Y
27.5
27.4
29.9
4.90
1.90
5.20
6.90
8.50
8.70
REE
629.46
674.70
930.00
150.18
245.71
368.70
45.77
66.77
19.60
Er Tm
R N
Yb
E-
O
O
6.54
AL
0.92
PR
F
Na2O
606.30
652.06
905.24
145.90
243.32
362.77
41.69
59.48
15.34
23.16
22.64
24.76
4.28
2.39
5.93
4.08
7.29
4.26
LREE/HREE
26.18
28.80
36.56
34.09
101.81
61.18
10.22
8.16
3.60
(La/Yb)N
46.14
51.24
72.24
48.02
268.42
140.14
8.75
11.42
1.98
(La/Sm)N
5.88
6.45
8.84
7.27
15.05
8.29
5.83
2.14
3.92
(Gd/Yb)N
3.70
3.67
3.58
3.03
5.85
5.98
0.91
3.37
0.43
δEu
0.70
0.71
0.53
0.88
1.52
0.73
0.91
0.88
0.80
δCe
1.02
1.02
1.02
1.33
1.05
1.18
1.01
0.91
0.99
(Ho/Yb)N
1.32
1.37
1.38
1.18
1.30
1.39
0.66
1.44
0.47
La/Sm
9.34
10.25
14.05
11.56
23.91
13.18
9.27
3.40
6.23
Y/Yb
12.73
12.86
12.89
10.43
10.56
12.38
7.84
11.97
6.69
JO
U
LREE
HREE
Rb
194
175
174
153
183
143
174
173
206
Ba
3120
2280
1748
803
1548
747
2485
7310
118
JOURNAL PRE-PROOF TLG-14
NO.
TLG-15
TLG-16
XFG-61
Biotite monzogranite porphyry
LJG-03
LJG-04
HY-01
Grante pegmatite
HY-02
HY-03
Granodiorite
27.3
25.2
63.4
21.6
21.3
42.5
18.05
3.63
24.5
U
3.22
2.59
3.34
0.77
0.45
0.84
4.85
1.56
14.4
K
36692
38186
38020
42005
53045
39016
37688
90069
32873
Ta
1.49
1.29
2.37
0.60
0.10
0.20
1.20
0.70
2.10
Nb
27.6
25.2
35.1
19.4
2.60
5.70
21.4
29.6
39.2
Sr
850
480
567
258
265
402
786
997
142
P
1266
1440
655
218
131
87
43.6
43.6
43.6
Zr
898
996
574
169
96.0
212
82.0
37.0
86.0
5.70
2.70
1.10
4.80
6.61
1.23
3.53
0.61
O
F
Th
19.6
21.5
13.9
5.00
2.50
15.8
15.8
17.7
2.89
2.99
Ti
5575
5935
3417
899
659
659
300
360
180
Cr
38.0
22.0
16.0
16.0
32.0
10.0
9.00
31.0
9.00
Ni
5.10
5.40
2.80
2.90
3.00
2.10
1.60
1.70
1.30
V
78.0
86.0
49.0
8.00
6.00
11.0
8.00
32.0
2.00
Ga
27.6
26.8
25.9
19.1
15.7
22.2
17.6
19.0
26.3
PR
E-
PR
O
Hf Sm
Table 3. Whole-rocks Rb–Sr and Sm–Nd isotopic compositions of granitic rocks in the giant Huayangchuan ore district. Sr
87Rb/86Sr
87Sr/86Sr
2σ
(87Sr/86Sr)i
Sm
Nd
147Sm/144Nd
143Nd/144Nd
2σ
(143Nd/144Nd)i
εNd(t)
fSm/Nd
4
904
0.006530
0.710008
0.000012
0.7100
5.34
36.0
0.089657
0.511712
0.000006
0.511572
-17.5
-0.54
4
855
0.005872
0.709844
0.000010
0.7098
4.48
29.6
0.091480
0.511669
0.000005
0.511589
-17.2
-0.53
8
935
0.005184
0.709784
0.000009
0.7098
5.31
35.4
0.090663
0.511668
0.000005
0.511590
-17.1
-0.54
1
932
0.005605
0.709875
0.000010
0.7099
5.28
33.1
0.096415
0.511675
0.000005
0.511591
-17.1
-0.51
4
786
0.006388
0.707682
0.000008
0.7077
1.23
6.60
0.112650
0.511970
0.000005
0.511798
-10.5
-0.43
3
997
0.005022
0.706236
0.000010
0.7062
3.53
14.7
0.145164
0.512259
0.000004
0.512038
-5.9
-0.26
6
142
0.042130
0.717851
0.000010
0.7177
0.61
2.80
0.131688
0.512012
0.000006
0.511811
-10.3
-0.33
3
258
0.017162
0.759095
0.000012
0.7586
2.89
20.5
0.085196
0.511058
0.000005
0.510045
-5.0
-0.57
3
265
0.019984
0.758527
0.000010
0.7580
2.99
30.7
0.058853
0.510652
0.000005
0.509953
-6.8
-0.70
3
402
0.010294
0.731005
0.000009
0.7307
6.61
52.9
0.075511
0.510938
0.000005
0.510041
-5.1
-0.62
4
850
0.006588
0.722726
0.000010
0.7226
15.8
107
0.089404
0.511004
0.000004
0.509941
-7.0
-0.55
480
0.010551
0.718197
0.000010
0.7179
15.8
113
0.084605
0.510952
0.000006
0.509945
-6.9
-0.57
567
0.008855
0.717815
0.000011
0.7176
17.7
134
0.079716
0.510882
0.000005
0.509934
-7.1
-0.59
4
R N
U
JO
5
AL
b
Tab. 4. Zircon Lu–Hf isotopic compositions of granitic rocks in the giant Huayangchuan ore district. No.
T(Ma)
176Yb/177Hf
2σ
176Lu/177Hf
2σ
176Hf/177Hf
2σ
(176Hf/177Hf)i
0.000207
0.000528
0.000006
0.281486
0.000009
0.281468
Biotite monzoranite porphyry TLG-14-01
1808
0.026696
176Yb/177Hf
2σ
176Lu/177Hf
2σ
176Hf/177Hf
2σ
(176Hf/177Hf)i
TLG-14-02
1808
0.048930
0.000147
0.000965
0.000006
0.281589
0.000011
0.281556
TLG-14-03
1808
0.044731
0.000121
0.000844
0.000003
0.281507
0.000010
0.281478
TLG-14-04
1808
0.058169
0.000075
0.001121
0.000002
0.281506
0.000009
0.281468
TLG-14-05
1808
0.042489
0.001007
0.000820
0.000015
0.281556
0.000011
0.281527
TLG-14-06
1808
0.060825
0.000440
0.001102
0.000004
0.281553
0.000011
0.281515
TLG-14-07
1808
0.065562
0.000198
0.001215
0.000002
0.281514
0.000010
0.281472
TLG-14-08
1808
0.088290
0.001101
0.001564
0.000013
0.281493
0.000011
0.281439
TLG-14-09
1808
0.048719
0.000306
0.000959
0.000001
0.281556
0.000011
0.281523
TLG-14-10
1808
0.067081
0.000164
0.001266
0.000003
0.281467
0.000010
0.281423
TLG-14-11
1808
0.066550
0.000426
0.001227
0.000006
0.281520
0.000011
0.281478
TLG-14-12
1808
0.030207
0.000354
0.000609
0.000003
0.281508
0.000011
0.281487
TLG-14-13
1808
0.046892
0.000339
0.000935
0.000007
0.281465
0.000010
0.281433
TLG-14-14
1808
0.056432
0.000225
0.001124
0.000009
0.281463
0.000010
0.281425
TLG-14-15
1808
0.028021
0.000196
0.000560
0.000001
0.281434
0.000010
0.281414
TLG-14-16
1808
0.038190
0.000135
0.000779
0.000005
0.281477
0.000011
0.281450
TLG-14-17
1808
0.070990
0.000107
0.001359
0.000004
0.281502
0.000011
0.281456
TLG-14-18
1808
0.082321
0.000274
0.001496
0.000003
0.281471
0.000011
0.281420
TLG-14-19
1808
0.023253
0.000121
0.000448
0.000001
0.281474
0.000009
0.281458
TLG-14-20
1808
0.062662
0.000336
0.001266
0.000010
0.281503
0.000011
0.281460
TLG-14-21
1808
0.041184
0.000770
0.000759
0.000011
0.281503
0.000009
0.281477
TLG-14-22
1808
0.042288
0.000049
0.000873
0.000002
0.281512
0.000014
0.281482
TLG-14-23
1808
0.043672
0.000592
0.000869
0.000014
0.281430
0.000011
0.281400
TLG-14-26
1808
0.033521
0.000370
0.000638
0.000004
0.281499
0.000010
0.281477
TLG-14-27
1808
0.029192
0.000155
0.000585
0.000001
0.281481
0.000011
0.281461
1808
0.051517
0.000419
0.000992
0.000004
0.281464
0.000009
0.281430
1808
0.059278
0.000264
0.001157
0.000008
0.281507
0.000010
0.281467
1808
0.030307
0.000149
0.000596
0.000001
0.281428
0.000010
0.281407
1808
0.027043
0.000501
0.000799
0.000012
0.281488
0.000016
0.281460
XFG-61-01
1807
0.047304
0.000327
0.001108
0.000009
0.281473
0.000011
0.281435
XFG-61-02
1807
0.021910
0.000029
0.000489
0.000001
0.281474
0.000008
0.281458
XFG-61-03
1807
0.046635
0.000131
0.001098
0.000001
0.281478
0.000010
0.281440
XFG-61-04
1807
0.044459
0.000158
0.001002
0.000006
0.281484
0.000011
0.281450
XFG-61-05
1807
0.026697
0.000251
0.000609
0.000004
0.281482
0.000011
0.281461
XFG-61-10
1807
0.067429
0.000094
0.001517
0.000004
0.281461
0.000011
0.281409
XFG-61-11
1807
0.031379
0.000127
0.000728
0.000004
0.281493
0.000010
0.281468
XFG-61-13
1807
0.074256
0.000311
0.001690
0.000012
0.281481
0.000012
0.281423
XFG-61-15
1807
0.045536
0.000343
0.000970
0.000010
0.281501
0.000008
0.281468
XFG-61-16
1807
0.040336
0.000586
0.000907
0.000016
0.281504
0.000009
0.281473
XFG-61-19
1807
0.054649
0.000549
0.001222
0.000015
0.281483
0.000007
0.281441
XFG-61-20
1807
0.050290
0.000458
0.001143
0.000013
0.281488
0.000008
0.281449
XFG-61-27
1807
0.028635
0.000213
0.000654
0.000006
0.281452
0.000007
0.281430
XFG-61-26
1807
0.038665
0.000098
0.000859
0.000003
0.281502
0.000008
0.281473
TLG-14-28 TLG-14-30
R N
TLG-14-31 TLG-14-32
O
PR
E-
PR
AL
No.
F
T(Ma)
O
JOURNAL PRE-PROOF
JO
U
Granite pegmatite
T(Ma)
176Yb/177Hf
2σ
176Lu/177Hf
2σ
176Hf/177Hf
2σ
(176Hf/177Hf)i
1807
0.040083
0.000104
0.000877
0.000003
0.281419
0.000008
0.281389
HY-01-01
233.3
0.083813
0.000697
0.002103
0.000009
0.282208
0.000008
0.282199
HY-01-03
233.3
0.106369
0.000407
0.002489
0.000010
0.282248
0.000010
0.282237
HY-01-07
233.3
0.080769
0.000915
0.001891
0.000011
0.282297
0.000009
0.282288
HY-01-08
233.3
0.107863
0.000636
0.002192
0.000008
0.281433
0.000013
0.281423
HY-01-10
233.3
0.073364
0.000359
0.001816
0.000012
0.282246
0.000009
0.282238
HY-01-11
233.3
0.045265
0.000846
0.000905
0.000016
0.281452
0.000009
0.281448
HY-01-13
233.3
0.129510
0.002863
0.003230
0.000074
0.282253
0.000015
0.282239
HY-01-14
233.3
0.078528
0.000247
0.002285
0.000009
0.282247
0.000013
0.282237
HY-01-18
233.3
0.098963
0.001486
0.002756
0.000029
0.282292
0.000009
0.282280
HY-01-21
233.3
0.115516
0.000758
0.003393
0.000037
0.282226
0.000012
0.282211
HY-01-24
233.3
0.082470
0.000886
0.001979
O
JOURNAL PRE-PROOF
0.000023
0.282274
0.000009
0.282265
HY-01-25
233.3
0.075510
0.000384
0.001985
0.000007
0.282290
0.000010
0.282282
HY-01-28
233.3
0.077053
0.000432
0.002325
0.000011
0.282282
0.000012
0.282271
HY-01-30
233.3
0.095211
0.001019
0.002670
0.000031
0.282275
0.000010
0.282263
HY-01-31
233.3
0.071545
0.000241
0.001731
0.000005
0.282220
0.000009
0.282213
HY-01-32
233.3
0.109937
0.000419
0.002494
0.000007
0.282295
0.000010
0.282284
No. XFG-61-28
O
PR
E-
PR
Biotite monzogranite
F
Granodiorite
132.3
0.053807
0.000783
0.001300
0.000021
0.282158
0.000009
0.282154
HYC-12-02
132.3
0.051532
0.000177
0.001318
0.000005
0.282047
0.000010
0.282044
HYC-12-03
132.3
0.031961
0.000293
0.000738
0.000007
0.282280
0.000009
0.282278
HYC-12-04
132.3
0.059660
0.000192
0.001529
0.000014
0.282188
0.000008
0.282185
HYC-12-05
132.3
0.033454
0.000275
0.000835
0.000006
0.282148
0.000008
0.282146
132.3
0.055091
0.000320
0.001409
0.000005
0.282154
0.000009
0.282150
132.3
0.032486
0.000510
0.000964
0.000019
0.281977
0.000011
0.281975
132.3
0.044486
0.000453
0.000945
0.000009
0.282261
0.000009
0.282259
HYC-12-09
132.3
0.018309
0.000124
0.000528
0.000004
0.281997
0.000008
0.281996
HYC-12-10
132.3
0.035196
0.000394
0.000862
0.000009
0.282133
0.000008
0.282131
HYC-12-11
132.3
0.025927
0.000068
0.000670
0.000002
0.281820
0.000008
0.281818
HYC-12-13
132.3
0.063024
0.000444
0.001973
0.000016
0.282161
0.000008
0.282157
HYC-12-14
132.3
0.045999
0.000181
0.001253
0.000007
0.282052
0.000008
0.282049
HYC-12-15
132.3
0.052236
0.000536
0.001133
0.000010
0.282275
0.000010
0.282272
HYC-12-16
132.3
0.042728
0.000228
0.001077
0.000005
0.282078
0.000007
0.282075
HYC-12-17
132.3
0.036000
0.000462
0.000837
0.000009
0.282114
0.000008
0.282112
HYC-12-18
132.3
0.041567
0.001017
0.001274
0.000034
0.281832
0.000009
0.281829
HYC-12-19
132.3
0.031240
0.000177
0.000835
0.000003
0.282023
0.000010
0.282021
HYC-12-21
132.3
0.027084
0.000045
0.000772
0.000002
0.282200
0.000008
0.282198
HYC-12-22
132.3
0.046977
0.000672
0.001651
0.000037
0.282042
0.000009
0.282038
HYC-12-23
132.3
0.047741
0.000600
0.001208
0.000010
0.282093
0.000008
0.282090
HYC-12-24
132.3
0.040395
0.000191
0.000978
0.000004
0.282087
0.000008
0.282084
HYC-12-25
132.3
0.034548
0.000448
0.000876
0.000007
0.282132
0.000008
0.282130
HYC-12-26
132.3
0.083433
0.000468
0.002364
0.000012
0.282109
0.000013
0.282103
HYC-12-06 HYC-12-07
JO
U
R N
HYC-12-08
AL
HYC-12-01
JOURNAL PRE-PROOF
No.
176Yb/177Hf
2σ
176Lu/177Hf
2σ
176Hf/177Hf
2σ
(176Hf/177Hf)i
132.3
0.037929
0.000108
0.000848
0.000001
0.282167
0.000008
0.282165
R N
AL
PR
E-
PR
O
O
F
HYC-12-27
T(Ma)
Highlights
U
(1) The Huayangchuan granitic rocks dated at ca. 1.8 Ga, ca. 233 Ma and ca. 132 Ma.
JO
(2) The granite pegmatite is locally associated with the Huayangchuan uranium
mineralization. (3) The
granodiorite is consistent with the main mineralization of the Huayangchuan deposit.
(4) The Huayangchuan granitic rocks are mainly sourced from the Taihua Group.
S0169-1368(19)30164-7 https://doi.org/10.1016/j.oregeorev.2019.103055 OREGEO 103055
To appear in:
Ore Geology Reviews
Received Date: Revised Date: Accepted Date:
22 February 2019 19 June 2019 31 July 2019
Please cite this article as: C. Yang, L. Zhao, H. Zheng, D. Wang, The multiple granitic magmatism in the giant Huayangchuan uranium polymetallic ore district: Implications for tectonic evolution of the southern margin of North China Craton in the Qinling Orogen, Ore Geology Reviews (2019), doi: https://doi.org/10.1016/j.oregeorev. 2019.103055
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© 2019 Published by Elsevier B.V.
JOURNAL PRE-PROOF
The
multiple
granitic
magmatism
in
the
giant
Huayangchuan
uranium
polymetallic
ore
district：
Implications for tectonic evolution of the southern margin of
O
F
North China Craton in the Qinling Orogen
Key Laboratory of Mineralogy and Metallogeny, Guangzhou Institute of Geochemistry, Chinese
Academy of Sciences, Guangzhou 510640, China
PR
a
O
Chunsi Yanga,b, Liandang Zhaoc*, Hui Zhenga,b, Dequan Wangd
University of Chinese Academy of Sciences, Beijing 100049, China
c
School of Earth Science and Resources, Chang’an University, Xi’an 710054, China
d
Sino Shaanxi Nuclear Industry Group, Xi’an 710100, China
*Corresponding
PR
E-
b
Author: Liandang Zhao
AL
School of Earth Science and Resources, Chang’an University, No. 126 Yanta Road, Yanta District, Xi’an 710054, China.
R N
Tel: +86 29 82339059.
JO
U
Email address: [email protected]
JOURNAL PRE-PROOF
Abstract The giant Huayangchuan U–Nb–Pb deposit in the Qinling Orogen is a newly verified carbonatite-hosted deposit in the southern margin of the North China Craton (NCC), central China.
F
Granitic magmatism is extensively developed in the Huayangchuan deposit area, but their ages
O
and petrogenesis are not well constrained. The exposed granitic rocks are mainly biotite
O
monzogranite porphyry, granite pegmatite, granodiorite, and biotite monzogranite with zircon U–
PR
Pb ages of 1808 ± 10 Ma, 1807 ± 14 Ma, 233 ± 1.4 Ma, and 132 ± 0.6 Ma, respectively. The Paleoproterozoic biotite monzogranite porphyry belongs to shoshonite and metaluminous series,
E-
showing enrichment of LREE and LILE and depletion of HREE and HFSE, with high Zr + Y
PR
+ Nb + Ce values and Ga/Al ratios, which are consistent with A-type granite. Whereas, the contemporaneous granite pegmatite dykes with weak mineralization are also cala-alkaline to
AL
shoshonite and peraluminous series, enriched in Rb, Ba, and LREE, and depleted in Nb, Ta, Ti and HREE. The shoshonite and weakly peraluminous Triassic granodiorite is slightly enriched
R N
in LREE with flat HREE patterns, enriched in Ba and Sr and depleted in Nb, Ta, P, and Ti, with similar geochemical characteristics to adakite-like rocks. The Early Cretaceous biotite
U
monzogranite is characterized by LREE enrichment and flat HREE patterns, belonging to
JO
shoshonite and metaluminous to weakly peraluminous I-type granite, with U and LILE enrichment, and HFSE-depleted. The high initial 87Sr/86Sr ratios and enriched Nd (εNd(t) = -17.5 to -17.1) and Hf (εHf(t) = -33.2 to -14.6) isotopes reveal that the Huayangchuan granitic rocks are obviously sourced from crustal-derived magmas. Combined with regional geology and this study, we proposed that: (1) the Paleoproterozoic biotite monzogranite porphyry and granite pegmatite were generated from ancient lower crust during post-collisional extension setting; (2) the
JOURNAL PRE-PROOF
granodiorite was likely sourced from partial melting of thickened lower crust with pelagic
sediments materials addition during the Triassic although the mineralization-related carbonatite having similar age with granodiorite may derive from mantle; and (3) the Early
F
Cretaceous biotite monzogranite was mainly sourced from the partial melting of lower crust
O
induced by the underplating of the mafic magma. We suggest that the first phase of magma
O
occurred in the Huayangchuan district during the Paleoproterozoic following the amalgamation of
PR
the Eastern and Western blocks along the Trans-North China Orogen. Since the Mesozoic, the ongoing northward subduction of the Yangtze Craton (YZC) resulted in the crust thickening,
E-
developing the Triassic granitic magmatism and major mineralization associated with carbonatite.
PR
The widespread Cretaceous granite and deposit in the southern margin of NCC indicate that intracontinental extension and lithospheric thinning occurred in response to the tectonic regime
AL
transition from NS-trending to EW-trending subduction.
R N
Keywords: Granitic magmatism; Geochemistry; Sr–Nd–Hf isotopes; Qinling Orogen;
JO
U
Huayangchuan U–Nb–Pb deposit
JOURNAL PRE-PROOF
1. Introduction Granitic rocks are widespread in the continental crust and many granitic rocks are closely associated to mineralization, including pegmatite-hosted rare metal deposits, granite-associated U
F
deposits, skarn Fe deposits, and porphyry Cu–Mo deposits (Kemp et al., 2007; Sial et al., 2011;
O
Yang et al., 2018). Studies on the geochronology, geochronology, and petrogenesis of granitic
O
rocks will offer some important clues not only to their geodynamic settings, but also the metal
PR
endowment mechanism (Barbarin, 1999; Chen et al., 2017; Sial et al., 2011).
The Qinling Orogen is one of the most important suture zones in the eastern Asia (Dong et al.,
E-
2013), which has undergone multi-stages of tectono-magmatic thermal events and recorded the
PR
opening, subduction, and closure of the northernmost Paleo-Tethys from the Early Paleozoic to the Mesozoic (Meng and Zhang, 2000). The southern margin of the North China Craton (NCC),
AL
located in the northern part of the Qinling Orogen, has undergone complex tectonic evolution and intensive magmatic activity. Dozens of medium to large scale Au deposits (e.g., Tongguan,
R N
Wenyu, Dongchuang, Yangzhaiyu, and Dahu), U deposit (e.g., Huayangchuan and Taoyuan), and Mo deposit (e.g., Jinduicheng, Huanglongpu, and Jiulong) concentrated in this area, constituting
U
the famous Qinling molybdenum metallogenic belt and the second largest Au-producing area in
JO
China. Several large granitic batholiths such as Laoniushan, Huashan, Wenyu, Niangniangshan, and Heyu and some small granite porphyries like Jinduicheng and Shijiawan developed in this region, with the latter generally thought to be closely related to especially the porphyry Mo mineralization but the former generally barren (e.g., Jinduicheng; Jiao et al., 2010; Zhu et al., 2010). However, recent explorations have identified several medium to large deposits spatially and temporally associated with the large granitic batholiths, e.g., Yuchiling porphyry Mo deposit
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(Li et al., 2009). The Huayangchuan U–Nb–Pb deposit is located in the Huayin County, Shaanxi Province. It was firstly discovered in the early 1970s and detailed exploration began in 2012 by the No. 224
F
Brigade, Sino Shaanxi Nuclear Industry Group. It has now been proven to be a world-class
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uranium deposit (detailed resource number is currently confidential). Previous studies generally
O
focused on the deposit geology, mineralogy, and geochemistry at Huayangchuan (Gao et al., 2017;
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Guo et al., 2008; He et al., 2016a, b; Hui and He, 2016; Hui et al., 2014; Wang et al., 2011; Wu et al., 2015; Xu, 2009, 2011; Xue et al., 2018; Yu, 1992). Few works has been done on multiphase of
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granitic magmatism, with the relationships between the granitic intrusions and mineralization, and
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tectonic evolution of the Huayangchuan ore district yet not well-documented. Thus, in this contribution, we present newly obtained zircon U–Pb ages and Hf isotope data, whole-rock major
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and trace elements, and whole-rock Sr–Nd isotopes for the granitic intrusions at Huayangchuan. When combined with previous geochemical studies, we will investigate petrogenesis of the
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granitic rocks and discuss the tectonic evolution for the Huayanchuan deposit and the southern
U
margin of the NCC.
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2. Regional and deposit geology 2.1 Regional geology The Qinling Orogen, sandwiching between the NCC and the Yangtze Craton (YZC) and
linking the Kunlun Orogen in the west and the Dabie Orogen in the east (Fig. 1a), is a worldrenowned Phanerozoic accretionary orogeny and undergone multi-stages of tectono-magmatic thermal events from the Archaean–Proterozoic to the Mesozoic (Dong et al., 2011; Li et al., 2015;
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Ratschbacher et al., 2003; Wu and Zheng, 2013; Zhang et al., 1995; Zheng et al., 2013). It is bounded by the Sanmenxia-Baofeng Fault to the north and the Longmenshan-Dabashan Fault to the south, and is divided into four major terranes or blocks from north to south, including the
F
southern margin of the NCC, the North Qinling Belt, the South Qinling Belt, and the northern
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margin of the YZC, by the Luonan-Luanchuan Fault and the Shangdan and the Mianlue sutures,
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respectively (Fig. 1b). The North Qinling Belt is predominately composed of the Proterozoic
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metasedimentary and metavolcanic rocks. The South Qinling Belt mainly contains Neoarchean– Neoproterozoic volcanic-sedimentary assemblages and overlain by Late Proterozoic to Triassic
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sedimentary sequences. The northern margin of the YZC is characterized by the Neoarchean
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crystalline basement and Mesoproterozoic–Neoproterozoic volcanic and sedimentary sequences, overlain by a thick Sinian to Mesozoic cover sequences (Zhang et al., 1995).
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The southern margin of the NCC, in which the Huayangchuan U–Nb–Pb deposit is located, is bounded by the Sanmenxia-Baofeng Fault to the north and the Luonan-Luanchuan Fault to the
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south, and consists mainly of Archaean (ca. 2.9–2.3Ga) basement and overlain by Proterozoic volcanic and sedimentary sequences (Zhang et al., 1995). The Archaean basement is composed of
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the amphibolite- to granulite-facies metamorphic rocks of the Taihua Group. The Proterozoic
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volcanic and sedimentary sequences comprise the Xiong’er Group, Guandaokou Group, and Luanchuan Group. The Xiong’er Group includes Paleoproterozoic mafic to felsic volcanic rocks with minor sedimentary rocks, whereas the Guandaokou Group consists of Mesoproterozoic quartzite and schist intercalated with dolomitic marble. The Neoproterozoic Luanchuan Group from the basement upwards, includes metasandstone of the Sanchuan Formation, marble and schist of the Nannihu Formation, and dolomitic marble of Meiyaogou Formation (Bao et al., 2014).
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A great amount of Late Paleoproterozoic to Mesoproterozoic intrusions had also developed in the southern margin of the NCC, including mafic dykes swarms (Bi et al., 2011; Wang et al., 2008), syenites and monzonites (Liu, 2011; Ren et al., 2000), and granitic rocks (Deng et al., 2015; Wang
F
et al., 2013). Late Paleozoic and Mesozoic granitic intrusions developed widely as large batholiths
O
and small porphyries in this region, which were explained as the results of collision and intraplate
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magmatism, respectively (Gao et al., 2014a, b; Mao et al., 2002). The major structures of the
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southern margin of the NCC are characterized by a series of nearly EW-trending faults, which mainly evolved from the Triassic to Jurassic southward thrusting and the Cretaceous northward
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normal faults (Li et al., 2011; Mao et al., 2002; Zhao et al., 2011, 2012). Moreover, the southern
al., 2004; Mao et al., 2008).
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2.2 Deposit geology
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margin of the NCC is an important Mo, Au, Ag, Pb–Zn, W, Sb, and U metallogenic belt (Chen et
The giant Huayangchuan U–Nb–Pb deposit is situated in the western part of the southern
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margin of the NCC (Fig. 1b) and is approximately 8 km to the north of the Huanglongpu Mo ore concentration area. The stratigraphy units in the Huayangchuan district are mainly the
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Sanguanmiao and Qincanggou formations of the Taihua Group and unconsolidated Quaternary
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sediments (Fig. 1c). The Sanguanmiao Formation mainly consists of amphibole–plagioclase gneiss intercalated with plagioclase gneiss, biotite–plagioclase gneiss, granitic gneiss, amphibole gneiss, and migmatite. The Qincanggou Formation is composed of amphibole–plagioclase gneiss intercalated with plagioclase gneiss, biotite–plagioclase gneiss, and granitic gneiss. The main geologic structures of the ore district are nearly NW-trending folds and NW-trending faults. The granitic igneous rocks outcropped in the deposit are mainly the larger plutons (e.g., Laoniushan,
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Huashan, and Xiaohe) and small dykes. The Laoniushan pluton is composed of Late Triassic granitoids, including quartz diorite, biotite monzogranite, quartz monzonite, and hornblende monzonite, and Late Jurassic to Early Cretaceous granitoids, including medium- to coarse-grained
F
and medium- to fined-grained biotite monzogranite (Ding et al., 2011; Qi et al., 2012). The
O
Huashan pluton consists of Late Triassic hornblende-bearing monzogranite and Early Cretaceous
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monzogranite and biotite monzogranite (Guo et al., 2009; Hu et al., 2012; Zhang et al., 2015). The
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Xiaohe pluton is Paleoproterozoic gneissic granite intercalated with light-color granitic dykes (Fig. 1c; Li, 2011).
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Based on field investigation and previous survey report, the orebodies-hosted carbonatite
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intruded into Archean–Paleoproterozoic metamorphic rocks of the Taihua Group and nearly parallel to the Huayangchuan Fault (Fig. 1c). Except for the carbonatite which hosted the major
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orebodies, the pegmatite dykes also contain minor mineralization at Huayangchuan (Gao et al., 2017). At Huayangchuan, U–Nb mineralization is associated with K-feldspar, actinolite, biotite,
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aegirine-pyroxene, and allanite alterations, whereas Pb mineralization is mainly correlated with
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pyrite, zeolite, and carbonate alterations.
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3. Sample descriptions The fine-grained biotite monzogranite porphyry crops out in the central part of the
Huayangchuan ore district, mainly occurred as NW-trending stocks in the Taihua Group. It has porphyritic texture, with phenocrysts of medium-grained K-feldspar and quartz. It contains quartz (~22 vol%), K-feldspar (~32 vol%), plagioclase(~30 vol%), biotite (~10 vol%), hornblende (~4 vol%), and accessory minerals (~2 vol%) of magnetite, zircon, and apatite (Fig. 2a and b). The
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plagioclase in matrix is partially replaced by sericite (Fig. 2c). The granite pegmatite is widely developed in the ore district and locally associated with the Huayangchuan uranium mineralization. The pale-white granite pegmatite contains quartz (~25
F
vol%), K-feldspar (45–48 vol%), plagioclase (15–20 vol%), and minor biotite (5–8 vol%), as well
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as accessory minerals (~2 vol%; Fig. 2d) of zircon, magnetite, and titanite. The coarse-grained K-
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feldspar is subhedral with cross-hatched twinning, and the plagioclase is subhedral and partially
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replaced by sericite (Fig. 2e).
The fine-grained granodiorite is observed in the northern part of ore district. The granodiorite
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is gray, and is composed of fine-grained quartz (~23 vol%), K-feldspar (20–24 vol%), plagioclase
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(40–45 vol%), biotite (4–8 vol%), and hornblende (~2 vol%), with accessory minerals (~2 vol%) of zircon, apatite, magnetite, titanite, and allanite (Fig. 2f). The plagioclase is euhedral to
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subhedral with polysynthetic twinning, whereas the K-feldspar is anhedral with cross-hatched twinning. The biotite was locally altered by chlorite. The hornblende commonly distributed as
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intergranular mineral between the feldspar and quartz (Fig. 2g). The medium- to fine-grained biotite monzogranite crops out in the western part of the ore
U
district. The biotite monzogranite is grey white, and contains medium-grained quartz (~22 vol%),
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K-feldspar (30–35% vol%), plagioclase (~30 vol%), and biotite (10–15% vol%), with accessory minerals (~3% vol%) of zircon, apatite, magnetite, and titanite (Fig. 2h). The K-feldspar is mainly subhedral with cross-hatched twinning, and the plagioclase is characterized by polysynthetic twinning and zonation (Fig. 2i).
4. Analytical methods
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4.1 Major and trace elements The whole-rock samples of the Huayangchuan granitic rocks for this study were crushed by jaw crusher and roller mill, and then powdered to less than 200-mesh using agate mortars in order
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to minimize potential contamination of transition metals. Major and trace elements were carried
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out at ALS Chemex (Guangzhou) Co. Ltd. The major element analyses were performed using X-
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ray fluorescence spectrometry (XRF), and the analytical precision is generally better than 2%. The
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trace and rare earth element abundances were determined with a X-series 2 ICP–MS. Precisions are better than 5% for elements in concentrations of more than 10 ppm, and better than 10% for
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elements in concentrations of less than 10 ppm. The detailed analytical procedures are described
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by Liu et al. (2008). The analytical uncertainties for the major elements were < 1%. The analytical accuracy was estimated by the relative difference between the measured and recommended values
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and was < 5% for most elements. 4.2 Sr–Nd isotope analyses
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Samples selected for Sr and Nd isotope analyses were dissolved in Teflon bombs with HF + HNO3 acid solution at 120 °C for 7 days. The solution was dried and re-dissolved in HCl solution
U
and then separated by conventional cation-exchange techniques. Sample preparation and chemical
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separation were as described by Liang et al. (2003). Sr–Nd isotope ratios were measured by MC– ICP–MS at the State Key Laboratory of Isotope Geochemistry, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences (GIGCAS). The total procedural blanks were in the range of 200–500 pg for Sr and ≤ 50 pg for Nd. Mass fractionation corrections for Sr and Nd isotope ratios are based on
86Sr/88Sr
= 0.1194 and
146Nd/144Nd
NIST SRM 987 and La Jolla standards yielding measured
= 0.7219, respectively, with the
87Sr/86Sr
and
143Nd/144Nd
ratios of
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0.710265 ± 12 (2σ) and 0.511862 ± 10 (2σ), respectively. 4.3 Zircon U–Pb dating Zircon grains were extracted by conventional heavy liquids and magnetic techniques, and
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then purified by hand picking under binocular microscope. Representative zircon grains were
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mounted in epoxy resin and polished down to expose the grain centre. Zircon U–Pb dating was
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carried out at the Key Laboratory of Mineralogy and Metallogeny, GIGCAS. The isotope and
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trace element compositions of zircon were in-situ measured by laser ablation inductively coupled plasma mass spectrometry (LA–ICP–MS) (Resonetics RESOlution S-155 laser + Agilent 7900)
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with a spot size of 29 μm. This laser ablation system is equipped with a large sample cell (155 mm
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× 105 mm), which can host 20 epoxy sample mounts (with diameter of 25.4 mm). It can wash out 99% signal within less than 1.5 s, because of its two-volume laser-ablation cell. A Squid
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smoothing device was used to reduce statistic error induced by laser-ablation pulses and improve the quality of data (Tu et al., 2011). Helium gas carrying the ablated sample aerosol is mixed with
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argon carrier gas and nitrogen as additional di-atomic gas to enhance sensitivity, and finally flows into ICP. Prior to analysis, the LA–ICP–MS system was optimized using NIST610 ablated with
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29 μm spot size and 5 μm/s scan speed to achieve maximum signal intensity and low oxide rate.
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Each analysis included approximately 20–30 s of back-ground acquisition (from a gas blank) followed by 50 s of data acquisition from the sample. 91500 zircon as the primary standard and Plesovice zircon as the secondary standard to calibrate the U–Pb age of zircon. The reference material (NIST 610) was used as external calibration reference and Si was used as the internal standard to quantify elemental concentrations in samples. The off-line selection and integration of the background and analyte signals, time-drift correction and quantitative calibration, were
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performed using ICPMSDataCal (Liu et al., 2008). 4.4 Zircon Hf isotope analyses All zircon Hf isotope analyses in this study were performed on a Neptune plus MC–ICP–MS
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(Thermo Scientific), coupled with a RESOlution M-50 193 nm laser ablation system (Resonetics),
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which are hosted at the State Key Laboratory of Isotope Geochemistry, GIGCAS. The detailed
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description of the two instruments can be found in Zhang et al. (2014). An X skimmer cone in the
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interface and a small flow of N2 (2 ml/L-1) were used to improve the instrumental sensitivity. All isotope signals are detected with Faraday cups under static mode. The laser parameters were set as
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follow: beam diameter, 45 μm; repetition rate, 6 Hz; energy density, ~4 J/cm-2. Helium was
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chosen as the carrier gas (800 ml/min-1). A “squid” smoothing device on the gas line to the ICP gives a smooth signal. Each analysis consisted of 400 cycles with an integration time of 0.131 s
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per cycle. The first 28 s was used to detect the gas blank with the laser beam off, followed by 30 s laser ablation for sample signals collection with laser beam on. During the measurement of this 180Hf
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study, the gas blank of isobaric interference of
and
176Lu
on
176Hf.
173Yb
175Lu
were used to correct the
The natural ratio values of
The mass bias factor of Yb is calculated from the measured
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and
176Yb/173Yb
and
used in the correction are 0.79381 (Segal et al., 2003) and 0.02656 (Wu et al., 2006).
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176Lu/175Lu
176Yb
was less than 0.2 mv.
173Yb/171Yb
and the natural ratio of
1.13268. The mass bias factor of Lu is assumed to be the same as that of Yb. The mass bias of 176Hf/177Hf
was normalized to
179Hf/177Hf
= 0.7325 with an exponential law. The detailed data
reduction procedure is reported in Zhang et al. (2015). 40 analyses of the Penglai zircon during the course of this study yielded a weighted mean of 176Hf/177Hf = 0.282907 ± 0.000035 (2σ), which is consistent within errors with the reported value in Li et al. (2010).
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5. Results 5.1 Zircon U–Pb geochronology
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LA–ICP–MS zircon U–Pb isotopic results of the fine-grained biotite monzogranite porphyry
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(TLG-14), granite pegmatite (XFG-61), fine-grained granodiorite (HY-01), and medium- to fine-
1
and
illustrated
on
the
concordia
diagrams
(Fig.
3).
The
representative
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Table
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grained biotite monzogranite (HYC-12) from the Huayangchuan ore district are listed in Appendix
cathodoluminescence (CL) images of zircon grains and analyzed spots with U–Pb ages and Lu–Hf
E-
isotope data are shown in Figure. 4. Zircon grains from all the samples are transparent, and
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euhedral to subeuhedral.
Zircon grains from the biotite monzogranite porphyry are 100 μm to 200 μm long and 50 μm
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to 150 μm wide, with length-to-width ratios of 1:1 to 2:1. They have oscillatory zoning in the CL images (Fig. 4a) and Th/U ratios of 0.85–2.50 (Appendix Tab. 1), suggesting a magmatic origin 206Pb/207Pb
ages ranging from
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(Belousova et al., 2002). Twenty-nine analyzed zircon grains had
1855 Ma to 1737 Ma, yielding a weighted mean 206Pb/207Pb age of 1808 ± 10 Ma (MSWD = 1.1;
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Fig. 3a).
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Zircon grains from the granite pegmatite are generally 150 μm to 300 μm long and 100 μm to
150 μm wide, with length-to-width ratios from 1.2:1 to 3:1. They have clear oscillatory zoning in the CL images (Fig. 4b), with Th/U ratios of 0.26–0.44 (Appendix Tab. 1). Analysis of twentytwo zircon grains had
206Pb/207Pb
ages ranging from 1857 Ma to 1765 Ma, yielding a weighted
mean 206Pb/207Pb age of 1807 ± 14 Ma (MSWD = 1.1; Fig. 3b). Zircon grains from the granodiorite are 200 μm to 300μm long and 50 um to 150 μm wide,
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with length-to-width ratios of 1.5:1 to 4:1. In the CL images (Fig. 4c), these zircons have clear oscillatory zoning with Th/U ratios of 0.24–0.40 (Appendix Tab. 1). All of the analyses plot along a concordia line (Fig. 3c), and two analyzed zircon spots (spot No. 8 and No. 11) had
207Pb/206Pb
age of 238 Ma to 230 Ma, with a weighted mean
age of 233.3 ± 1.4 Ma (MSWD = 1.1; Fig. 3e).
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206Pb/238U
206Pb/238U
age (Fig. 3d).
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Another thirteen grains yielded
206Pb/238U
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concordia line and has not been used to calculate the weighted mean
F
ages of 2313 ± 26 Ma and 1835 ± 25 Ma, respectively. One zircon grain deviates from the
Zircon grains from the biotite monzogranite are 100 μm to 300 μm long, 80 μm to 150 μm
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wide with length-to-width ratios of 1:1 to 3:1. The zircon grains have clear oscillatory zoning in
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CL images (Fig. 4d) and Th/U ratios of 0.16–1.39 (Appendix Tab. 1). Twenty-seven analyzed zircons yielded 206Pb/238U ages ranging from 135 Ma to 131 Ma, forming a concordant population
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with a weighted mean 206Pb/238U age of 132.3 ± 0.6 Ma (MSWD = 0.5; Fig. 3f). 5.2 Major and trace elements
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The whole-rock major and trace elements analytical results of the representative granitic rocks samples in the Huayangchuan ore district are shown in Appendix Table 2.
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The fine-grained biotite monzogranite porphyry has SiO2 contents of 60.04–67.87 wt.%,
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Al2O3 contents of 14.35–16.00 wt.%, K2O contents of 4.42–4.60 wt.%, Na2O contents of 4.12– 5.21 wt.%, CaO contents of 1.35–3.29 wt.%, Fe2O3T contents of 4.66–7.74 wt.%, and MgO contents of 0.72–1.48 wt.%, with low Mg# values of 23–28. On the SiO2 vs. Nb/Y diagram (Fig. 5a), most samples plot in alkali granite and monzonite fields. The biotite monzogranite porphyries are shoshonite series (Fig. 5b) and metaluminous (Fig. 5c) with A/CNK values of 0.89–0.97. The biotite monzogranite porphyry is enriched in LREE and depleted in HREE with (La/Yb)N values
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of 46.14–72.24, having negative Eu anomalies (δEu = 0.53–0.71; Fig. 6a). On the primitivenormalized trace element diagram (Fig. 6b), all of the samples show enrichment in the LILE (e.g., Rb, Ba, and Th) and depletion in HFSE (e.g., Nb, Ta, and Ti).
F
The granite pegmatite has high SiO2 (72.54–72.93 wt.%), K2O (4.70–6.39 wt.%), Na2O
O
(2.65–3.82 wt.%), and Al2O3 (13.99–14.06 wt.%) contents, and low CaO (0.47–1.12 wt.%), MgO
O
(0.23–0.38 wt.%), and Fe2O3T (1.38–2.39 wt.%) contents, with A/CNK ratios of 0.77–1.11 and
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Mg# values of 16–31. They show cala-alkaline and shoshonite affinities, and belong to metaluminous to weakly peraluminous granite (Fig. 5b and c). The granite pegmatite is LREE-
E-
enriched and HREE-depleted, with (La/Yb)N values of 48.08–268.42, and has variable Eu
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anomalies with δEu values of 0.73–1.52 (Fig. 6c). All the samples are enriched in Rb and Ba, and depleted in Nb, Ta, and Ti (Fig. 6d).
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The fine-grained granodiorite has SiO2 contents of 68.42–74.66 wt.%, K2O contents of 3.96– 4.54 wt.%, plotting in alkali granite field (Fig. 5a) with shoshonite affinity (Fig. 5b). They have
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Al2O3 contents of 13.96–15.43 wt.% and are peraluminous with A/CNK ratios of 1.03–1.04. They also have Na2O contents of 4.96–5.15 wt.%, MgO contents of 0.07–0.16 wt.%, Fe2O3T contents of
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0.98–1.27 wt.%, and Mg# values of 11–20. The granodiorite is slightly enriched in LREE
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((La/Yb)N = 1.98–11.42), having flat HREE patterns ((Gd/Yb)N = 0.43–0.91) and weakly negative Eu anomalies with δEu values of 0.80–0.91 (Fig. 6e). They are depleted in Nb, Ta, and Ti, and enriched in Ba and Sr (Fig. 6f). The medium- to fine-grained biotite monzogranite has high SiO2 (70.50–71.40 wt.%) and K2O + Na2O contents (8.57–8.77 wt.%), plotting into the alkali granite field (Fig. 5a). They have K2O contents of 4.14–4.43 wt.%, Na2O contents of 4.22–4.37 wt.%, Al2O3 contents of 14.66–
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15.53 wt.%, CaO contents of 1.89–1.99 wt.%, and K2O/Na2O ratios of 0.95–1.04 with A/CNK ratios of 0.97–1.01, plotting in the shoshonite field (Fig. 5b) and belonging to metaluminous to weakly peraluminous granite (Fig. 5c). They have MgO contents of 0.31–0.37 wt.%, Fe2O3T
F
contents of 2.19–2.47 wt.%, and Mg# values of 22–26. All the samples display consistent REE
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patterns (Fig. 6g), and are characterized by LREE enrichment and flat HREE patterns ((La/Yb)N =
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24.74–32.07, (Gd/Yb)N = 2.11–2.58; Appendix Tab. 2), having weakly negative Eu anomalies
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with δEu values of 0.86–0.92. They are also enriched in U and LILE, and depleted in HFSE (Fig. 6h).
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5.3 Sr–Nd isotopes
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The whole-rock Rb–Sr and Sm–Nd isotope results are listed in Appendix Table 3 and shown in Figure 7a and b. The initial
87Sr/86Sr
isotopic ratios and εNd(t) values for the biotite
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monzogranite porphyry, granite pegmatite, granodiorite, and biotite monzogranite were calculated based on their corresponding zircon U–Pb ages. They have initial
87Sr/86Sr
values of 0.7194–
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0.7226, 0.7307–0.7586, 0.7062–0.7177, and 0.7098–0.7100, with corresponding negative εNd(t) values of -7.1 to -6.9, -6.8 to -5.1, -10.5 to -5.9, and -17.5 to -17.1, and two-stage Nd model
U
(TDM2) ages of 2874–2856 Ma, 2845–2701 Ma, 1865–1485 Ma, and 2317–2246 Ma, respectively 87Sr/86Sr
values,
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(Appendix Tab. 3). Comparatively, the granite pegmatite has higher initial
suggesting that it can be easily influenced by later magma activity or alteration events. These granitic rocks are mostly deviated from mantle array and plot in the field of the Taihua Group (Fig. 7a and b), especially in the Neoarchean–Paleoproterozoic Taihua Group evolution domain of the εNd(t)–t evolution diagram (Fig. 7b). 5.4 Zircon Hf isotopes
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Zircon Lu–Hf isotope were determined on the same or similar domains of the zircon grains dated for U–Pb ages in this study. The analytical results are listed in Appendix Table 4 and illustrated in Figure 7c. These zircons yielded 176Hf/177Hf ratios of 0.281400–0.281566, 0.281389–
F
0.281473, 0.281423–0.282388, and 0.281281–0.282280 for the biotite monzogranite porphyry,
O
granite pegmatite, granodiorite, and biotite monzogranite, respectively. Their corresponding εHf(t)
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values of -8.7 to -8.2, -8.7 to -5.7, -15.4 to -8.5, and -33.2 to -14.6, with two-stage Hf model
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(TDM2) ages of 2977–2636 Ma, 3002–2817 Ma, 2239–1800 Ma, and 3277–2111 Ma, respectively (Appendix Tab. 4). All the analyzed spots plot below the depleted mantle and the chondritic
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uniform reservoir lines, similar to the zircons from the Taihua metamorphic complex (Fig. 7c).
6. Discussion
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6.1 Timing of granitic magmatism
Three pulses of granitic magmatism were identified in the Huayangchuan ore district,
R N
including the Early Proterozoic (ca. 1808 Ma), the Early Mesozoic (ca. 233 Ma), and Late Mesozoic (ca. 132 Ma). Our new LA–ICP–MS zircon U–Pb age of the biotite monzogranite
U
porphyry (1808 ± 10 Ma) is consistent with LA–ICP–MS zircon U–Pb ages of 1803–1797 Ma for
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the Guijiayu monzogranite reported in Deng et al. (2016) and SIMS zircon U–Pb ages of 1829– 1827 Ma for the A-type granite reported by Xue et al. (2018) in the Huayangchuan area. The firstly-reported LA–ICP–MS zircon U–Pb age of 1807 ± 14 Ma for the granite pegmatite in our study broadly distributed in Huayangchuan, further indicates that the Early Proterozoic granitic magmatism was widely developed in the southern margin of the NCC. Based on observations, the spatial relationship between the granite pegmatite dykes and U mineralization could be
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sporadically observed, suggesting that emplacement of the granite pegmatite dykes probably contributed to preliminary enrichment of uranium mineralization at Huayangchuan. Hu et al. (2012) reported a LA–ICP–MS zircon U–Pb age of 205 ± 2 Ma for the Wengyu
F
granite of the Huashan pluton and Qi et al. (2012) gained LA–ICP–MS zircon U–Pb ages of 223 ±
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1 Ma, 222 ± 1 Ma, and 214 ± 1 Ma for adamellite, granodiorite, and coarse-grained biotite
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monzogranite of the Laoniushan pluton, respectively. Moreover, mineralization events during the
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Indosinian have been well documented in the southern margin of the NCC, such as the Huanglongpu carbonatite-hosted Mo deposit (ca. 221 Ma; Zhao et al., 2010), the Dashigou
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carbonatite-hosted Mo deposit (ca. 216 Ma; Hu, 2013), the Xigou feldspar-quartz vein-hosted Mo
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deposit (ca. 212 Ma; Yuan et al., 2014), and the Dahu orogenic lode Au–Mo deposit (ca. 218 Ma; Li et al., 2008). In this study, we obtain a LA–ICP–MS zircon U–Pb age of 233.3 ± 1.4 Ma for the
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granodiorite in the Huayangchuan ore district. The giant Huyangchuan U polymetallic deposit is mainly related to carbonatite which shares similar characteristics with the Huanglongpu
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carbonatite-hosted Mo deposit. Integrating the former published regional ages and this study, we propose that the main mineralization period of the Huayangchuan deposit may be formed in the
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Indosinian.
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Early Cretaceous granites emplaced in the southern margin of the NCC were also
documented, including the Huashan pluton (ca. 146–132 Ma; Hu et al., 2012; Mao et al., 2005; Zhang et al., 2015; Guo et al., 2009), Heyu pluton (ca. 134–127 Ma; Guo et al., 2009; Mao et al., 2005), Laoniushan pluton (ca. 152–146 Ma; Qi et al., 2012; Zhu et al., 2008), Niangniangshan pluton (ca. 142–139 Ma; Gao et al., 2012; Mao et al., 2005), and Wenyu pluton (ca. 138–135 Ma; Gao et al., 2012; Mao et al., 2005). Some Mo mineralization-related granitic magmatism also have
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been reported in the southern margin of the NCC, such as Shijiawan granite porphyry (141 ± 0.6 Ma; Zhao et al., 2010) and Jinduicheng granite porphyry (143.7 ± 3 Ma; Jiao et al., 2010). The biotite monzogranite in the Huayangchuan ore district was formed at 132.3 ± 0.6 Ma, consistent
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with former reported Late Mesozoic magmatism in this region, although no Mo mineralization
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was observed in the Huayangchuan biotite monzogranite.
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6.2 Petrogenesis
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6.2.1 The Paleoproterozoic biotite monzogranite porphyry and granite pegmatite
The fine-grained biotite monzogranite porphyry has relatively high K2O contents of 4.42–
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4.58 wt.% (> 4 wt.%), Zr + Nb + Ce + Y contents of 1196–1460 ppm (> 350 ppm), FeOT/(FeOT +
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MgO) ratios of 0.81–0.85 (> 0.8), and 10000 Ga/Al ratios of 3.16–3.41 (> 2.6), consistent with Atype granite (Frost et al., 2001; Whalen et al., 1987; Zhang et al., 2012). The presence of
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interstitial Fe-oxide-bearing minerals (e.g., magnetite, hornblende, and biotite; Fig., 2c) also implies an A-type granite character (Bonin, 2007; Landenberger and Collions, 1996). On the Zr vs.
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10000 Ga/Al diagram (Fig. 8a), all the samples plot in the A-type granite field, and can be further classified as A1-type granite (Fig. 8b).
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Various A-type granites worldwide can be attributed to three main petrogenetic scenarios,
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including (1) extreme differentiation of mantle-derived tholeiitic or alkaline basaltic magma precursor (Mushkin et al., 2003; Turner et al., 1992); (2) partial melting of crustal rocks (Bonin, 2007; Huang et al., 2011; King et al., 1997; Whalen et al., 1987); and (3) combined crustal and mantle sources, in the form either of crustal assimilation and fractional crystallization (AFC) of mantle-derived magmas, or mixing between mantle-derived and crustal magmas (Kemp et al., 2005; Yang et al., 2006; Zhang et al., 2012). In general, fractional crystallization of a mantle-
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derived magma produces rocks with peralkaline compositions (King et al., 1997; Patiño, 1997; Wu et al., 2002). Obviously, the metaluminous nature of the biotite monzogranite porphyries (Fig. 5c) is inconsistent with the chemical signatures of mantle-derived A-type granite. So the partial
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melting of crustal rocks and interactions between mantle-derived magma and crustal rocks are
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likely considered to be the most possible mechanisms for the biotite monzogranite porphyry. The
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higher calculated zircon saturation temperatures (892–916 °C) may indicate that lower crustal
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sources was underplated and heated by mantle-derived mafic magmas to form the biotite monzogranite porphyry. In fact, although coeval ~1.8 Ga mafic dykes have been well documented
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in the Xiaoqinling gold district (Bi et al., 2011), the negative εNd(t) and εHf(t) values, in
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combination with the absence of mafic enclaves in the pluton and low Mg# values probably favor that the underplating of mafic magma in the lower crustal may have only provided the heat source
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for the formation of the biotite monzogranite porphyry. The Neoarchean to Paleoproterozoic basement rocks of the Taihua Group are widespread in
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this region. The older two-stage Nd (2874–2856 Ma) and Hf model ages (2977–2636 Ma) of the biotite monzogranite porphyry overlap with the ages of the Taihua Group (ca. 2.9–2.3 Ga; Diwu et 87Sr/86Sr
values of 0.7194–0.7226
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al., 2018). The biotite monzogranite porphyry has high initial
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and negative εNd(t) values of -7.1 to -6.9, which plot in the field of the Taihua Group (Fig. 7a) and follow the trend of Neoarchean–Paleoproterozoic Taihua Group evolution (Fig. 7b). Furthermore, the zircon εHf(t) values of the biotite monzogranite porphyries are plotted in the evolution field of rocks from the Taihua Group (Fig. 7c), also implying that they were most likely derived from partial melting of the basement rocks of the Taihua Group. In summary, the underplating of mafic magmas may have provided heat to induce the partial melting of the Taihua Group and generated
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the Huayangchuan biotite monzogranite porphyry. The granite pegmatite dykes in Huayangchuan ore district have temporal and spatial relationships with the biotite monzogranite porphyry, as well as similar age and geochemical
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characters, i.e., U–Pb age of 1807 ± 14 Ma, negative εNd(t) and εHf(t) values of -6.79 to -4.99 and
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-8.7 to -6.7, and the corresponding two-stage Nd and Hf model ages of 2845–2701 Ma and 3002–
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2817 Ma, which suggest that they may have the same petrogenesis, i.e., partial melting of ancient
6.2.2 The Triassic granodiorite
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lower crust.
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The fine-grained granodiorite is characterized by weakly negative Eu anomalies (δEu = 0.80–
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0.91), with relatively high Sr contents, low Y and Yb contents, and high Sr/Y and (La/Yb)N ratios, which is similar to adakite-like rocks (Fig. 9a; Defant and Drummond, 1990).
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Several genetic models have been summarized to account for the origin of adakites and adakitic rocks (Long et al., 2011 and references therein), including (1) partial melting of a
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subducting basaltic slab; (2) partial melting of the slab-melt-modified peridotitic mantle wedge; (3) crustal assimilation and fractional crystallization (AFC) processes of parental basaltic magmas; (4)
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partial melting of delaminated lower crust; and (5) partial melting of thickened lower crust. Based
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on the regional and geochemical characteristics of the fine-grained granodiorite, we propose that they were formed by partial melting of thickened lower crust with the following reasons: (1) the Huayangchuan granodiorite is characterized by high SiO2 and K2O contents, low MgO contents and low Mg# values (Appendix Tab. 2), which are different from those of typical slab-derived adakites (Martin et al., 2005); (2) zircons from the granodiorite exhibit strongly negative εHf(t) values, which indicates a significant contribution of old crustal material and preclude an origin
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through partial melting of the slab-melt-modified peridotitic mantle wedge (Martin et al., 2005; Moyen et al., 2001; Stern and Kilian et al., 1996); (3) most adakites formed by crustal assimilation and fractional crystallization (AFC) from coeval parental basaltic magma under high pressure are
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intermediate and mafic rocks, as basic magmas are unable to directly form high-silicic rocks. This
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process would generate a large number of mafic rocks in the surrounding area. However, the
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regional studies indicate that the exposed area of contemporaneous basalt is quite small (Bi et al.,
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2011); and (4) some studies indicate that adakitic rocks produced by partial melting of delaminated lower crust should exhibit increased MgO, TiO2, and compatible element abundances
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due to metasomatism of mantle peridotite (e.g. Cr, Co, and Ni) and modified Nd–Hf isotopic
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systems of the adakitic melts (Castillo, 2006; Chung et al., 2003; Kay and Kay, 1993). Thus, adakitic rocks derived from partial melting of delaminated lower crust are likely to show higher
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Mg#, εNd(t), and εHf(t) values than primitive melts of lower crust. However, low MgO and TiO2 contents and compatible element abundances, combined with low Mg#, εNd(t), and εHf(t) values,
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suggest that the granodiorite are unlikely to have been derived from partial melting of delaminated lower crust. Two inherent zircons were found from the granodiorite in this study, and have ages of 2313 ± 26 Ma and 1835 ± 25 Ma, respectively. In combination with negative
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207Pb/206Pb
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εHf(t) values and older two-stage Hf model ages, which may suggest that they were likely generated from the Paleoproterozoic crustal materials and inherited during formation of the Triassic granodiorite. Low contents of Y and HREE in granodiorite rocks indicate that garnet or hornblende may act as residual mineral in magmatic source. Garnet is strongly compatible for HREE and hornblende is relatively compatible for MREE. Hence, when garnet is the main residual mineral in
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magmatic source, the HREE will show strongly fractionated patterns (Y/Yb > 10, (Ho/Yb)N > 1.2; Ge et al., (2002), whereas when hornblende is the main residual mineral in magmatic source, the MREE will show flat patterns (Y/Yb ≈ 10, (Ho/Yb)N ≈ 1.0; Ge et al., 2002). The Huayangchuan
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granodiorite has Y/Yb and (Ho/Yb)N ratios of 6.69–11.97 and 0.47–1.44, respectively, suggesting
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that hornblende should be the most important residual mineral and only minor garnet in magmatic
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source. Previous experimental results suggested that the garnet-in curve was located between 9
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Kbar and 14 Kbar in terms of the various compositions of basaltic sources at 800–1000 ℃ (Vielzeuf and Schmidt, 2001). The presence of minor garnet as residual minerals in the
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granodiorite source indicates the pressure condition should correspond to the garnet-in curve
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nearby, approximately 9–12 Kbar (30–40 km in depth). Noteworthy, the content of Sr in the granodiorite exhibit a widely range of variation, suggesting that a high Sr–Ba magma source, so
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the Taihua Group basement rocks cannot to be the single source to produce the Huayangchuan granodiorote. Plank and Langmuir (1998) argued that the variation of Sr should be strongly
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attributed to carbonate contribution as a result of that may be influenced by biological productivity and/or hydrothermal processes. Therefore, pelagic sediments material was probably added during
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the process of the granodiorite magma generation. This view is likely reinforced by the formation
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of coeval Dashigou and Yuantou carbonatite-hosted Mo deposit in the Huanglongpu ore field, which derived directly from metasomatized sub-continental lithosphere mantle and exhibited an EM1-type isotopic signature (Song et al., 2015; Xu et al., 2011). As discuss above, we conclude that the granodiorite were derived from partial melting of the ancient basement materials of the Taihua Group and contaminated by pelagic sediments-bearing subducted materials. 6.2.3 The Early Cretaceous biotite monzogranite
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The medium- to fine-grained biotite monzogranite has Na2O contents of 4.22–4.37 wt.% and A/CNK ratios of 0.97–1.01, which are in accordance with the basic feature of I-type granites defined by Chappell and White (1974), i.e., Na2O > 3.2 wt.% and A/CNK < 1.1. However, the
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biotite monzogranite samples have higher SiO2 (> 70% wt.%) and low P2O5 contents (< 0.11 wt.%;
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Appendix Tab. 2), and show metaluminous to weakly peraluminous characteristics (Fig. 5c). The
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Huayangchuan biotite monzogranite is recognized as highly fractionated I-type granites by the
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following evidences, including (1) the calculated amounts of corundum in CIPW norm calculations of the biotite monzogranite is absence (C < 1%), which is in accordance with
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characteristics of the I-type granites (Chappell and White, 2001); (2) a typical negative correlation
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between decreasing Na2O and P2O5 and increasing Si2O (Fig. 10a and b; Chappell, 1999; Green and Watson, 1982; Harrison and Watson, 1984; Li et al., 2007; Watson, 1979; Watson and
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Capobianco, 1981; Wolf and London, 1994); and (3) high contents of Th and Y, showing a positive correlation with Rb (Fig. 10c-d; Chappell, 1999; Clemens, 2003; Li et al., 2007).
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The biotite monzogranite has relatively high Y/Yb and (Ho/Yb)N ratios of 11.10–11.50 and 1.04–1.18, respectively, suggesting that garnet remained as residual minerals in the source after
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melt extraction (Ge et al., 2002). Negative Eu anomalies with δEu values of 0.83–0.85 imply
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fractional crystallization of plagioclase during the magmatic evolution or plagioclase retention in the magma source. The I-type biotite monzogranite has higher SiO2 contents and relatively lower MgO contents and Mg# values, exhibiting a crustal origin affinity. Zircons of the biotite monzogranite show negative εHf(t) values (-33.2 to -14.6) and relatively older TDM2(Hf) ages (3277–2111 Ma), also suggesting that they were probably derived from ancient lower crust, which is consistent with their negative εNd(t) values of -17.5 to -17.1 and correspondingly old TDM2(Nd)
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ages of 2317–2246 Ma. A role for crustal-derived magmas in the formation of the biotite monzogranite is also suggested by their Y/Yb ratios of 10.94–11.58 (crustal source of Y/Yb > 2; Eby 1992) and Zr/Hf ratios of 34.8-35.2 (crustal source of Zr/Hf > 33; Taylor and Mclennan,
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1985). However, the biotite monzogranite has Nb/Ta ratios of 16.5-18.8, which suggests an origin
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of mantle materials (~17.5 for typical primitive mantle; Green, 1995). These evidences may
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suggest that the biotite monzogranite was formed by melting of ancient lower crust with a minor
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contribution of the mantle.
6.3 Implications for geodynamic settings at Huayangchuan and Qinling Orogen
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The formation and evolution of the Qinling Orogen has undergone three different stages, i.e.,
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(1) Stage I presents the formation of the Neoarchean–Paleoproterozoic and Mesoproterozoic crystalline basement and transitional metamorphic basement; (2) Stage II presents a
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Neoproterozoic to Middle Triassic major orogenic period that was controlled by plate tectonics and vertical accretion regimes; and (3) Stage III presents a period of Mesozoic and Cenozoic post-
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orogenic intracontinental tectonic evolution (Zhang et al., 1995). Although A-type granites were originally thought to form in rift zones or stable continental
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blocks (Loiselle and Wones, 1979), they can also form in both anorogenic and post-orogenic
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settings (Bonin, 1990; Eby, 1992; Pitcher, 1997; Sylvester, 1989; Whalen et al., 1987). On the tectonic discrimination diagrams of Rb vs. (Y+Nb) and R2 vs. R1, all the samples plot in the fields of post-collisional granites (Fig. 11a) and late orogenic granites (Fig. 11b). In addition, the biotite monzogranite porphyries exhibit high-K calc-alkaline affinity, which is consistent with the granites that formed in the orogenic belts associated with the late stage of continental collision (Barbarin, 1999). The fine-grained biotite monzogranite porphyry at Huayangchuan yields a U–Pb
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age of 1808 Ma, which is slightly later than the amalgamation of the eastern and western blocks of the NCC along the Trans-North China Orogen at ca. 1.85 Ga (Liu et al., 2009; Song et al., 1996; Zhao, 2001; Zhai et al., 2005). During this period, granitic rocks with ages of ca. 1.8 Ga were
F
widely distributed in the NCC (Deng et al., 2016; Gao et al., 2013; Geng et al., 2004, 2006; Liu et
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al., 2014; Wang et al., 2010; Xue et al., 2018; Zhao and Zhou, 2009; Zhao et al., 2008) and mafic
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dykes and volcanic rocks of similar ages also have been recognized in the southern margin of the
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NCC (Bi et al., 2011; Wang et al., 2008; Zhao et al., 2004), which generally show no evidence of deformation and metamorphism and consistent with anorogenic or post-orogenic magmatism.
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Alternatively, they may be linked to extensional setting after the amalgamation of the NCC along
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the Trans-North China Orogen. The coeval granite pegmatite at Huayangchuan has a consistent spatial and temporal correlation with the biotite monzogranite porphyry, suggesting that they were
AL
likely emplaced in the same tectonic setting. The upwelling of asthenosphere resulted in partial melting of lower crust could be triggered by underplating of mantle-derived magma or
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lithospheric delamination (Fan et al., 2001; Lu et al., 2006; Muir et al., 1995; Petford and Atherton, 1996; Zhang et al., 2002). The granitic porphyry has MgO and Mg# values of 0.72–1.48 wt.% and
U
23–29, respectively, which is inconsistent with the magma formed by lithospheric delamination.
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Therefore, we draw a conclusion that underplating of mantle-derived magma induced partial melting of the Taihua Group and formed the biotite monzogranite porphyry and granite pegmatite. During the Late Triassic to Early Cretaceous, the NCC and the YZC collided and resulted in
the formation of the Qinling Orogen (Chen, 2010; Dong et al., 2012 and references therein). In the Triassic, the eastern part of the Qinling Orogen underwent deep continental subduction when the YZC subducted beneath the NCC (Zhu et al., 2011), and the Qinling Paleo-Tethys finally closed
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in a westward zipper-like way at ca. 230–200 Ma (Chen, 2010). In this study, we obtained a U–Pb age of 233 Ma for the granodiorite at Huayangchuan, which is corresponding to Mesozoic and Cenozoic post-orogenic intracontinental tectonic evolution of the Qinling Orogen (Fig. 11a and b).
F
They have identical crystallization ages with Late Triassic granites in the South Qinling (Gong et
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al., 2009a, b; Qin et al., 2009, 2010; Sun et al., 2002), North Qinling (Lu et al., 1996; Gong et al.,
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2009a; Zhang et al., 2009), and West Qinling (Zhang et al., 2006, 2007), and mineralization in the
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southern of the NCC (Li et al., 2008; Zhao et al., 2010; Zhu et al., 2011; Hu, 2013; Yuan et al., 2014). Meanwhile, the metamorphic ages of ca. 242–221 Ma for the Mianlue ophiolite (Li et al.,
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1996) and ca. 240–216 Ma for the Mianlue blueschist (Mattauer et al., 1985; Yin et al., 1991) in
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the East Qinling are consistent with the metamorphic ages of 240 Ma to 225 Ma for the UHP metamorphic rocks in the Dabie-Sulu orogenic belt (Zheng et al., 2009). Accordingly, we argued
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that the granodiorite at Huayangchuan was likely formed in a post-collisional setting. In this period, the lithosphere was strongly compressed and thickened, inducing to the partial melting of
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lower crust to form the granodiorite.
Since Late Mesozoic, the Qinling Orogen was spatially located in the conjugation site of the
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India, Eurasian, and Pacific plates, and significantly influenced by the Pacific Plate. At ca. 145 Ma,
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the Qinling Orogen underwent a tectonic transition in subduction direction from NS-trending to EW-trending (Lu, 1998; Ren, 1991; Zhao et al., 1994), which resulted in the large-scale Late Mesozoic magmatism and mineralization throughout the Qinling Orogen caused by lithospheric extension and thinning. The biotite monzogranite in the Huayangchuan ore district has a U–Pb age of 132 Ma, which is slightly younger than peak ages of tectonic regime transition. Based on this study and the available geological data, the Qinling region has evolved into an intracontinental
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extensional setting during the Early Cretaceous. Hence, we can conclude that the biotite monzogranite was likely emplaced in an extension setting, resulting from partial melting of the lower crust induced by the underplating of the mafic magmas, with minor addition of mantle
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material.
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7. Conclusions
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(1) Three pules of magmatism were identified in the Huayangchuan uranium polymetallic deposit: ca. 1.8 Ga fine-grained biotite monzogranite porphyry and granite pegmatite, ca. 233 Ma
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fine-grained granodiorite, and ca. 132 Ma medium- to fine-grained biotite monzogranite.
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(2) The biotite monzogranite porphyries (ca. 1808 Ma) and granite pegmatite (ca. 1807 Ma) have enriched Nd and Hf isotopes (εNd(t) <0; εHf(t) <0) and old two-stage Nd (2874–2856 Ma) and
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Hf model ages (2977–2636 Ma), indicating that they were generated from ancient lower crust during post-collision extension setting.
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(3) The granodiorites are similar to adakite-like rocks, and have high Sr and Ba contents and negative εNd(t) and εHf(t) values, suggesting that they were derived from partial melting of the
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thickened ancient crust of the Taihua Group and contaminated pelagic sediments-bearing
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materials.
(4) The biotite monzogranites belong to I-type granites and were probably sourced from the
partial melting of lower crust induced by the underplating of the mafic magmas during an extension setting in response to tectonic regime transition from NS-trending to EW-trending.
Acknowledgements
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This study was funded by the joint research project of Guangzhou Institute of Geochemistry, Chinese Academy of Sciences and Sino Shaanxi Nuclear Industry Group (No. Y631141001). We are grateful to the No. 224 Brigade Co. Ltd., Sino Shaanxi Nuclear Industry Group for assistance
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in field work. We thank Dr. Dan Wu and Dr. Le Zhang for zircon U–Pb dating and Sr–Nd–Hf
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isotope analyses, respectively. Comments from two anonymous reviewers are also very helpful to
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us to better present our results and discussion in this manuscript.
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Xu, C., Song, W.L., Qi, L., Wang, L.J., 2009. Geochemical characteristics and tectonic setting of ore-bearing carbonatites in Huanglongpu Mo ore field. Acta Petrol. Sin. 25, 422–430 (in Chinese with English abstract).
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Xu, C., Taylor, R.N., Kynicky, J., Chakhmouradian, A.R., Song, W.L., Wang, L.J., 2011. The origin of enriched mantle beneath North China block: Evidence from young carbonatites. Lithos 127, 1–9.
F
Xue, S., Xu, Y., Ling, M.X., Kang, Q.Q., Jiang, X.Y., Sun, S.J., Wu, K., Zhang, Z.K., Luo, Z.B.,
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Liu, Y.L., Sun, W.D., 2018. Geochemical constraints on genesis of Paleoproterozoic A-type
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granite in the south margin of North China Craton. Lithos 304–307, 489–500.
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Yang, J.B., Zhao, Z.D., Hou, Q.Y., Niu, Y.L., Mo, X.X., Sheng, D., Wang, L.L., 2018. Petrogenesis of Cretaceous (133–84 Ma) intermediate dykes and host granites in southeastern
E-
China: Implications for lithospheric extension, continental crustal growth, and geodynamics
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of Palaeo–Pacific subduction. Lithos 296–299, 195–211.
Yang, J.H., Wu, F.Y., Chung, S.L., Wilde, S.A., Chu, M.F., 2006. A hybrid origin for the
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Qianshan A–type granite, northeast China: geochemical and Sr–Nd–Hf isotopic evidence. Lithos 89, 89–106.
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Yin, Q., Jagoutz, E., Kroner, A., 1991. Precambrian (?) blueschist/coesite bearing eclogite belt in central China. Terra Abstracts 3, 85–86.
U
Yu, X.H., 1992. Geological, petrol–mineralogical characteristics and origin of the carbonatites
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from Huayangchuan, shaanxi province. Earth Sci. 17, 151–159 (in Chinese with English abstract).
Yuan, H.C., Wang, R.T., Jiao, J.G., Li, W.X., Liu, W.Q., Tan, W., 2014. Re–Os isotopic ages of molybdenites from Xigou Mo deposit in Huaxian of East Qinling and their geological significance. J. Earth Sci. and Environ. 36, 120–117 (in Chinese with English abstract). Zhai, M.G., Guo, J.H., Liu, W.J., 2005. Neoarchean to Paleoproterozoic continental evolution and
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tectonic history of the North China Craton. J. Asian Earth Sci. 24, 547–561. Zhang, G.W., Zhang, Z.Q., Dong, Y.P., 1995. Nature of main tectono–lithostratigraphic units of the Qinling Orogen: Implications for the tectonic evolution. Acta Petrol. Sin. 11, 101–114 (in
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Zhang, H.F., Sun, M., Zhou, X.H., Fan, W.M., Zhai, M.G., Yin, J.F., 2002. Mesozoic lithosphere
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destruction beneath the North China Craton: Evidence from major, trace element, and Sr-Nd-
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Zhang, H.F., Jin, L.L., Zhang, L., Harris, N., 2007. Geochemical and Pb–Sr–Nd isotopic
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Zhang, H.F., Zhang, B.R., Harris, N., Zhang, L., Chen, Y.L., Chen, N.S., Zhao, Z.D., 2006. U–Pb
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constraints on petrogenesis and tectonic affinity. J. Asian Earth Sci. 27, 751–764. Zhang, L., Ren, Z.Y., Nichols, A.R.L., Zhang, Y.H., Zhang, Y., Qian, S.P., Liu, J.Q., 2014. Lead
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Zhang, L., Ren, Z.Y., Xia, X.P., Li, J., Zhang, Z.F., 2015. IsotopeMaker: A Matlab program for isotopic data reduction. Int. J. Mass Spectrom. 392, 118–124.
Zhang, L., Yang, R.S., Mao, S.D., Lu, Y.H., Qin, Y., Liu, H.J., 2009. Sr and Pb isotope geochemistry and ore-forming material source of the Yangshan gold deposit. Acta Petrol. Sin. 25, 2811–2822 (in Chinese with English abstract).
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craton–orogen. Lithos 144–145, 12–23.
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Zhao, G.C., 2001. Paleoproterozoic assembly of the North China Craton. Geol. Mag. 138, 87–91.
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Zhao, G.C., Wilde, S.A., Sun, M., Li, S.Z., Li, X.P., Zhang, J., 2008. SHRIMP U–Pb zircon ages of granitoid rocks in the Lüliang Complex: implications for the accretion and evolution of the
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Zhao, H.X., Frimmel, H.E., Jiang, S.Y., Dai, B.Z., 2011. LA–ICP–MS trace element analysis of pyrite from the Xiaoqinling gold district, China: Implications for ore genesis. Ore Geol. Rev. 43, 142–153.
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U
Jinduicheng porphyry Mo deposit in the East Qinling, China, and Its metallogenetic
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geodynamical setting. Acta Geol. Sin. 82, 204–220 (in Chinese with English abstract).
Zhu, L.M., Zhang, G.W., Guo, B., Le, B., Gong, H.J., Wang, F., 2010. Geochemistry of the Jinduicheng Mo-bearing porphyry and deposit, and its implications for the geodynamic setting in East Qinling, P.R. China. Chem. Erde-Geochem. 70, 159–174. Zhu, L.M., Zhang, G.W., Chen, Y.J., Ding, Z.J., Guo, B., Wang, F., Lee, B., 2011. Zircon U–Pb ages and geochemistry of the Wenquan Mo-bearing granitioids in West Qinling, China:
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Constraints on the geodynamic setting for the newly discovered Wenquan Mo deposit. Ore Geol. Rev. 39, 46–62. Zindler, A., Hart, S.R., 1986. Chemical geodynamics. Ann. Rev. Earth Planet. Sci. Lett. 14, 493–
O
F
571.
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Figure captions
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Fig. 1. (a) The tectonic map of China, showing the location of the Qinling Orogen (after Chen et al., 2009). (b) Tectonic subdivision of the Qinling Orogen (after Zhang et al., 2007). (c) Simplified
PR
E-
geological map of the Huayangchuan deposit (after Gao et al., 2017).
Fig. 2. Hand specimen photograph and representative photomicrograph of the granitic rocks in the
AL
Huayangchuan ore district. (a–c) Biotite monzogranite porphyry. (d–e) Granite pegmatite. (f–g) Granodiorite. (h–i) Biotite monzogranite. Abbreviations: Bt: biotite, Hbl: hornblende, Kfs: K-
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feldspar, Mt: magnetite, Pl: plagioclase, Q: quartz.
JO
U
Fig. 3. Zircon U–Pb concordia diagrams for granitic rocks in the Huayangchuan ore district.
Fig. 4. The representative zircon CL images for granitic rocks in the Huayangchuan ore district.
Fig. 5. Major and trace element diagram for the granitic rocks in the Huayangchuan ore district. (a) SiO2 vs. Nb/Y diagram (after Maniar and Piccoli, 1994). (b) Th/Yb vs. Ta/Yb diagram (after Muller, 1992). (c) A/NK vs. A/CNK diagram (after Maniar and Piccoli, 1989).
JOURNAL PRE-PROOF
Fig. 6. Chondrite-normalized REE distribution patterns and primitive-mantle normalized trace element variation diagrams for the granitic rocks in the Huayangchuan ore district. Normalized
87Sr/86Sr
diagram (a, after Zindler and Hart, 1986), εNd(t) vs. time (Ma)
O
Fig. 7. εNd(t) vs. initial
O
F
values are from Sun and Mcdonough (1989).
PR
diagram (b, after Zhao et al., 2012), and εHf(t) vs. age diagram (c, after Hu et al., 2012) for the granitic rocks. εNd(t) and εHf(t) fields of the Taihua Group are from Zhao et al. (2012) and
PR
E-
references therein and Deng et al. (2016), respectively.
Fig. 8. (a) Zr vs. 10000Ga/Al discrimination diagram for the granitic rocks in the Huayangchuan
AL
ore district (after Whalen et al., 1987). (b) Distinguishing diagram between A1 and A2 type
R N
granites (after Eby, 1992).
Fig. 9. (La/Yb)N vs. YbN diagram (a, after Defant and Drummond, 1990) and La/Sm vs. La
U
diagram (b, after Allègre and Minster, 1978) for the granitic rocks in the Huayangchuan ore
JO
district.
Fig. 10. Chemical variation diagrams for the granitic rocks in the Huyangchuan ore district. (a) Na2O vs. SiO2 (after Chappell and White, 1992). (b) P2O5 vs. SiO2 (after Chappell and White, 1992). (c) Th vs. Rb (after Chappell, 1999). (d) Y vs. Rb (after Chappell, 1999).
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Fig. 11. Diagrams of tectonic discrimination for the granitic rocks in the Huyangchuan ore district. (a) Rb vs. (Y+Nb) (after Pearce et al., 1984); (b) R2 vs. R1 (after Batchelor and Bowden, 1985). Abbreviations: syn-COLG = syn-collisional granites; VGA = volcanic-arc granites; ORG = ocean-
F
ridge granites; WPG = within-plate granites; Post-COLG = post-collisional granites. Tectonic
O
areas from Fig. 11b with numbers are representing mantle fractions, pre-plate collision, post-
PR
– 11(Na + K) – 2(Fe + Ti); and R2 = 6Ca + 2Mg + Al.
O
collision uplift, late-orogenic, anorogenic, syn-collision and post-orogenic, respectively. R1 = 4Si
E-
Table captions
AL
Huayangchuan ore district.
PR
Table 1. LA–ICP–MS zircon U–Pb isotopic compositions of granitic rocks in the giant
Table 2. Major (wt.%), trace, and earth element (ppm) compositions of granitic rocks in the giant
R N
Huayangchuan ore district.
U
Table 3. Whole-rocks Rb–Sr and Sm–Nd isotopic compositions of granitic rocks in the giant
JO
Huayangchuan ore district.
Table 4. Zircon Lu–Hf isotopic compositions of granitic rocks in the giant Huayangchuan ore district.
JO
U
R N
AL
PR
E-
PR
O
O
F
JOURNAL PRE-PROOF
JO
U
R N
AL
PR
E-
PR
O
O
F
JOURNAL PRE-PROOF
JO
U
R N
AL
PR
E-
PR
O
O
F
JOURNAL PRE-PROOF
JO
U
R N
AL
PR
E-
PR
O
O
F
JOURNAL PRE-PROOF
JO
U
R N
AL
PR
E-
PR
O
O
F
JOURNAL PRE-PROOF
JO
U
R N
AL
PR
E-
PR
O
O
F
JOURNAL PRE-PROOF
JO
U
R N
AL
PR
E-
PR
O
O
F
JOURNAL PRE-PROOF
O
O
F
JOURNAL PRE-PROOF
TLG-14
Pb
Th
U
Th/U
Biotite monzogranite porphyry 223
191
1.16
TLG-14-02
120
265
206
1.28
TLG-14-03
87.0
179
166
1.08
TLG-14-04
114
213
TLG-14-05
108
191
TLG-14-06
133
380
TLG-14-07
115
239
TLG-14-08
219
TLG-14-09
1σ
206Pb/238U
1σ
207Pb/206Pb
0.1132
0.0018
5.0846
0.0950
0.3238
0.0041
1851
0.1130
0.0018
5.2796
0.0941
0.3364
0.0037
1850
0.1111
0.0017
5.0227
0.0891
0.3257
0.0037
1818
203
1.05
0.1134
0.0016
5.3574
0.0901
0.3397
0.0033
1855
225
0.85
0.1106
0.0016
4.8616
0.0731
0.3172
0.0034
1810
189
2.02
0.1097
0.0017
5.0289
0.0858
0.3302
0.0036
1794
213
1.12
0.1084
0.0017
5.1021
0.0883
0.3391
0.0039
1773
620
338
1.84
0.1063
0.0017
4.7539
0.0812
0.3221
0.0034
1737
121
279
213
1.31
0.1075
0.0018
4.9074
0.0880
0.3287
0.0035
1767
TLG-14-10
237
623
389
1.60
0.1079
0.0016
4.8514
0.0783
0.3237
0.0033
1765
TLG-14-11
159
461
221
2.09
0.1077
0.0016
4.9557
0.0820
0.3313
0.0034
1761
TLG-14-12
89.7
192
162
1.19
0.1124
0.0019
5.1670
0.0962
0.3309
0.0034
1839
TLG-14-13
114
266
188
1.42
0.1094
0.0015
5.1630
0.0860
0.3399
0.0040
1791
TLG-14-14
123
272
212
1.28
0.1087
0.0016
5.0750
0.0810
0.3366
0.0037
1789
TLG-14-15
68.8
158
120
1.31
0.1110
0.0018
5.1196
0.0915
0.3320
0.0033
1817
TLG-14-16
215
524
343
1.53
0.1085
0.0015
5.0356
0.0786
0.3341
0.0033
1776
TLG-14-17
131
291
231
1.26
0.1114
0.0018
5.1246
0.0892
0.3312
0.0036
1833
TLG-14-18
114
270
185
1.45
0.1114
0.0017
5.2492
0.0946
0.3389
0.0039
1833
TLG-14-19
161
400
285
1.40
0.1098
0.0016
4.8391
0.0787
0.3168
0.0030
1796
TLG-14-20
211
581
304
1.91
0.1109
0.0015
5.1376
0.0816
0.3332
0.0036
1815
TLG-14-21
272
843
338
2.50
0.1103
0.0015
5.1154
0.0750
0.3335
0.0031
1806
TLG-14-22
99.3
233
162
1.44
0.1123
0.0018
5.2438
0.0886
0.3362
0.0038
1839
TLG-14-23
161
444
244
1.82
0.1111
0.0017
5.0568
0.0827
0.3277
0.0035
1817
TLG-14-26
73.8
155
131
1.19
0.1104
0.0019
5.3323
0.1015
0.3478
0.0047
1806
TLG-14-27
63.2
151
108
1.40
0.1123
0.0020
5.2610
0.1064
0.3378
0.0047
1839
TLG-14-28
75.2
172
130
1.32
0.1115
0.0018
5.1955
0.0878
0.3360
0.0034
1833
TLG-14-30
185
535
256
2.09
0.1105
0.0016
5.1034
0.0774
0.3330
0.0032
1809
JO
R N
AL
PR
102
1σ
207Pb/235U
U
TLG-14-01
Isotope ratio
207Pb/206Pb
E-
Element(ug/g)
Spot
PR
Table 1. LA–ICP–MS zircon U–Pb isotopic compositions of granitic rocks in the giant Huayangchuan ore district.
JOURNAL PRE-PROOF Element(ug/g)
Spot
Th/U
Isotope ratio 207Pb/206Pb
Pb
Th
U
TLG-14-31
163
389
287
1.35
0.1111
0.0016
TLG-14-32
119
261
213
1.23
0.1106
0.0017
XFG-61
1σ
207Pb/235U
1σ
206Pb/238U
1σ
207Pb/206Pb
4.9862
0.0768
0.3236
0.0032
1818
5.1061
0.0836
0.3328
0.0034
1810
Granite pegmatite 386
304
997
0.30
0.1132
0.0020
5.3288
0.0976
0.3378
0.0034
1851
XFG-61-02
134
107
358
0.30
0.1124
0.0019
5.1495
0.0969
0.3289
0.0040
1839
XFG-61-03
448
459
1128
0.41
0.1135
0.0017
5.2427
0.0880
0.3316
0.0037
1857
XFG-61-04
488
476
1245
0.38
0.1135
0.0016
5.1872
0.0838
0.3280
0.0033
1855
XFG-61-05
240
193
618
0.31
0.1135
0.0016
5.2579
0.0832
0.3327
0.0033
1857
XFG-61-10
373
293
970
0.30
0.1120
0.0019
5.2078
0.0952
0.3348
0.0038
1831
XFG-61-11
271
221
692
0.32
0.1122
0.0018
5.2644
0.0952
0.3373
0.0036
1836
XFG-61-12
332
254
852
0.30
0.1108
0.0017
5.1903
0.0825
0.3371
0.0030
1813
XFG-61-13
462
453
1129
0.40
0.1097
0.0015
5.2097
0.0788
0.3419
0.0031
1794
XFG-61-14
292
306
731
0.42
0.1097
0.0016
5.0396
0.0833
0.3308
0.0035
1794
XFG-61-15
319
343
789
0.44
0.1094
0.0016
4.9650
0.0848
0.3266
0.0035
1791
XFG-61-16
335
243
871
0.28
0.1087
0.0016
5.0727
0.0894
0.3359
0.0037
1789
XFG-61-17
369
284
966
0.29
0.1081
0.0019
4.9911
0.0971
0.3327
0.0038
1769
XFG-61-18
449
392
1124
0.35
0.1083
0.0017
5.0123
0.0858
0.3339
0.0032
1770
XFG-61-19
323
235
857
0.27
0.1088
0.0016
4.9913
0.0842
0.3310
0.0033
1789
XFG-61-20
281
191
XFG-61-21
281
242
XFG-61-22
351
275
XFG-61-25
232
203
XFG-61-26
371
XFG-61-27 XFG-61-28
O
O
PR
PR
E-
0.26
0.1088
0.0016
5.0254
0.0867
0.3332
0.0033
1789
695
0.35
0.1079
0.0016
5.0121
0.0801
0.3358
0.0031
1765
900
0.31
0.1075
0.0016
4.9362
0.0826
0.3318
0.0031
1767
602
0.34
0.1087
0.0020
4.8780
0.1057
0.3244
0.0041
1789
329
934
0.35
0.1087
0.0019
4.8931
0.0975
0.3252
0.0038
1789
224
171
561
0.31
0.1096
0.0018
5.0675
0.0891
0.3342
0.0029
1794
406
380
973
0.39
0.1100
0.0017
5.2061
0.0905
0.3417
0.0034
1799
AL
740
Granodiorite 133
904
3347
0.27
0.0510
0.0009
0.2656
0.0048
0.0376
0.0004
242.7
HY-01-03
177
1485
4379
0.34
0.0523
0.0008
0.2718
0.0053
0.0374
0.0005
298.2
HY-01-07
191
1266
4831
0.26
0.0553
0.0013
0.2888
0.0092
0.0370
0.0005
433.4
HY-01-08
321
458
522
0.88
0.1471
0.0023
8.1881
0.1425
0.4005
0.0043
2313
HY-01-10
113
752
2867
0.26
0.0519
0.0010
0.2658
0.0053
0.0369
0.0005
283.4
HY-01-11
315
912
449
2.03
0.1121
0.0016
5.0136
0.0810
0.3221
0.0035
1835
HY-01-13
146
1215
3657
0.33
0.0518
0.0008
0.2678
0.0051
0.0373
0.0005
276.0
HY-01-14
103
663
2639
0.25
0.0555
0.0014
0.2877
0.0086
0.0370
0.0004
435.2
HY-01-18
127
1002
3333
0.30
0.0510
0.0008
0.2583
0.0045
0.0365
0.0004
239.0
HY-01-21
132
958
3301
0.29
0.0562
0.0010
0.2818
0.0044
0.0364
0.0003
461.2
HY-01-22
198
1834
4532
0.40
0.0654
0.0013
0.3396
0.0081
0.0371
0.0003
787.0
HY-01-25
137
1063
3490
0.30
0.0492
0.0009
0.2516
0.0050
0.0368
0.0004
166.8
HY-01-28
114
835
3048
0.27
0.0516
0.0009
0.2615
0.0058
0.0363
0.0005
333.4
HY-01-30
118
742
3066
0.24
0.0538
0.0014
0.2782
0.0080
0.0370
0.0004
364.9
HY-01-31
97.5
600
2460
0.24
0.0551
0.0015
0.2878
0.0088
0.0374
0.0004
416.7
HY-01-32
106
684
2712
0.25
0.0542
0.0011
0.2724
0.0049
0.0364
0.0004
376.0
JO
HY-01-01
U
R N
HY-01
F
XFG-61-01
JOURNAL PRE-PROOF Element(ug/g)
Spot HYC-12
Pb
Th
U
Isotope ratio
Th/U
207Pb/206Pb
1σ
207Pb/235U
1σ
206Pb/238U
1σ
207Pb/206Pb
Biotite monzonitic granite 21.7
637
699
0.91
0.0484
0.0017
0.1394
0.0050
0.0209
0.0003
120.5
HYC-12-02
21.4
353
920
0.38
0.0484
0.0017
0.1376
0.0050
0.0207
0.0003
116.8
HYC-12-03
8.70
237
326
0.73
0.0469
0.0026
0.1322
0.0072
0.0208
0.0004
42.7
HYC-12-04
17.0
301
699
0.43
0.0498
0.0018
0.1427
0.0051
0.0208
0.0002
183.4
HYC-12-05
11.0
279
426
0.65
0.0505
0.0024
0.1464
0.0077
0.0211
0.0004
216.7
HYC-12-06
10.6
234
439
0.53
0.0495
0.0026
0.1400
0.0072
0.0207
0.0004
172.3
HYC-12-07
17.3
208
781
0.27
0.0489
0.0016
0.1428
0.0055
0.0211
0.0004
142.7
HYC-12-08
8.25
287
230
1.25
0.0487
0.0030
0.1372
0.0077
0.0208
0.0004
200.1
HYC-12-09
10.6
181
418
0.43
0.0496
0.0023
0.1410
0.0066
0.0209
0.0004
172.3
HYC-12-10
21.7
199
988
0.20
0.0513
0.0017
0.1464
0.0050
0.0207
0.0002
253.8
HYC-12-11
12.5
95.9
587
0.16
0.0503
0.0018
0.1465
0.0057
0.0211
0.0004
209.3
HYC-12-12
66.7
1258
2462
0.51
0.0501
0.0012
0.1465
0.0035
0.0211
0.0002
198.2
HYC-12-13
23.3
280
1091
0.26
0.0507
0.0015
0.1428
0.0043
0.0205
0.0003
227.8
HYC-12-14
19.7
218
927
0.24
0.0491
0.0016
0.1394
0.0047
0.0206
0.0002
150.1
HYC-12-15
22.6
873
626
1.39
0.0500
0.0020
0.1413
0.0056
0.0205
0.0003
198.2
HYC-12-16
29.4
539
1225
0.44
0.0503
0.0016
0.1450
0.0049
0.0209
0.0003
209.3
HYC-12-17
40.8
865
1644
0.53
0.0483
0.0013
0.1371
0.0039
0.0205
0.0002
122.3
HYC-12-18
24.1
279
1100
0.25
0.0493
0.0015
0.1404
0.0044
0.0206
0.0002
161.2
HYC-12-19
14.6
117
691
0.17
0.0508
0.0016
0.1469
0.0047
0.0208
0.0002
235.3
HYC-12-20
40.1
551
1761
0.31
0.0492
0.0011
0.1418
0.0036
0.0207
0.0003
153.8
HYC-12-21
21.8
174
1038
0.17
0.0464
0.0012
0.1324
0.0035
0.0206
0.0002
16.8
HYC-12-22
27.5
551
1115
0.49
0.0483
0.0013
0.1393
0.0041
0.0208
0.0003
122.3
HYC-12-23
18.6
219
826
0.26
0.0482
0.0015
0.1391
0.0045
0.0209
0.0003
109.4
HYC-12-24
24.2
306
1091
0.28
0.0493
0.0014
0.1392
0.0040
0.0205
0.0002
161.2
HYC-12-25
15.1
118
738
0.16
0.0499
0.0016
0.1441
0.0051
0.0209
0.0003
187.1
HYC-12-26
16.9
552
531
1.04
0.0495
0.0020
0.1404
0.0054
0.0207
0.0002
172.3
HYC-12-27
7.34
67.5
345
0.20
0.0505
0.0022
0.1438
0.0063
0.0207
0.0003
216.7
O
O
PR
E-
PR
AL
U
R N
F
HYC-12-01
JO
Table 2. Major (wt.%), trace and earth element (ppm) compositions of granitic rocks in the giant Huayangchuan ore district. NO.
TLG-14
TLG-15
TLG-16
XFG-61
Biotite monzogranite porphyry
LJG-03
LJG-04
HY-01
Grante pegmatite
HY-02
HY-03
Granodiorite
SiO2
61.19
60.04
67.87
72.54
72.66
72.93
73.51
68.42
74.66
TiO2
0.93
0.99
0.57
0.15
0.11
0.11
0.05
0.06
0.03
Al2O3
15.61
16.00
14.35
14.06
13.99
14.07
14.35
15.43
13.96
TFe2O3
6.70
7.74
4.66
2.39
1.38
2.37
0.98
1.27
1.13
MnO
0.08
0.09
0.10
0.05
0.04
0.05
0.04
0.04
0.06
MgO
1.37
1.48
0.72
0.38
0.31
0.23
0.07
0.16
0.07
CaO
3.29
2.44
1.35
0.47
1.12
1.00
0.43
0.18
0.41
JOURNAL PRE-PROOF
NO.
TLG-14
TLG-15
TLG-16
XFG-61
Biotite monzogranite porphyry
LJG-03
LJG-04
HY-01
Grante pegmatite
HY-02
HY-03
Granodiorite
4.12
5.21
4.49
3.82
2.65
3.69
4.96
1.66
5.15
K2O
4.42
4.60
4.58
5.06
6.39
4.70
4.54
10.85
3.96
P2O5
0.29
0.33
0.15
0.05
0.03
0.02
0.01
0.01
0.01
LOI
0.91
0.44
0.34
0.58
0.60
0.91
0.37
0.48
0.40
Total
98.91
99.36
99.18
99.55
99.28
100.08
99.31
98.56
99.84
K2O+Na2O
8.54
9.81
9.07
8.88
9.04
8.39
9.50
12.51
9.11
K2O/Na2O
1.07
0.88
1.02
1.32
2.41
1.27
A/CNK
0.89
0.89
0.97
1.11
1.05
1.08
A/NK
1.35
1.18
1.16
1.19
1.24
A.R.
2.65
3.27
3.74
4.14
3.98
R1
1387
854
1724
2227
R2
726
648
462
Mg#
29
27
23
La
148
162
248
Ce
301
325
459
Pr
32.4
34.5
44.5
Nd
107
113
Sm
15.8
15.8
Eu
2.85
2.86
2.34
Gd
9.85
9.65
Tb
1.19
1.17
Dy
5.73
Ho
0.77
1.03
1.04
1.03
1.26
1.10
1.06
1.09
3.51
4.60
9.07
4.46
2366
2385
2047
1398
2188
345
410
394
PR
331
330
321
24
31
16
12
20
11
33.4
71.5
87.1
11.4
12.0
3.80
82.2
126
198
20.2
24.9
7.20
6.26
11.2
17.6
1.93
3.42
0.76
134
20.5
30.7
52.9
6.60
14.7
2.80
17.7
2.89
2.99
6.61
1.23
3.53
0.61
0.65
0.98
1.08
0.33
0.93
0.17
10.3
1.76
1.30
3.10
0.99
2.95
0.69
1.23
0.19
0.11
0.31
0.15
0.38
0.12
5.48
6.25
1.04
0.47
1.25
0.89
1.85
0.80
0.98
1.00
1.10
0.19
0.08
0.20
0.20
0.35
0.21
2.54
2.51
2.83
0.47
0.19
0.51
0.70
0.83
0.73
0.36
0.36
0.42
0.07
0.03
0.07
0.12
0.12
0.16
2.16
2.13
2.32
0.47
0.18
0.42
0.88
0.71
1.30
Lu
0.35
0.34
0.36
0.09
0.03
0.07
0.15
0.10
0.25
Y
27.5
27.4
29.9
4.90
1.90
5.20
6.90
8.50
8.70
REE
629.46
674.70
930.00
150.18
245.71
368.70
45.77
66.77
19.60
Er Tm
R N
Yb
E-
O
O
6.54
AL
0.92
PR
F
Na2O
606.30
652.06
905.24
145.90
243.32
362.77
41.69
59.48
15.34
23.16
22.64
24.76
4.28
2.39
5.93
4.08
7.29
4.26
LREE/HREE
26.18
28.80
36.56
34.09
101.81
61.18
10.22
8.16
3.60
(La/Yb)N
46.14
51.24
72.24
48.02
268.42
140.14
8.75
11.42
1.98
(La/Sm)N
5.88
6.45
8.84
7.27
15.05
8.29
5.83
2.14
3.92
(Gd/Yb)N
3.70
3.67
3.58
3.03
5.85
5.98
0.91
3.37
0.43
δEu
0.70
0.71
0.53
0.88
1.52
0.73
0.91
0.88
0.80
δCe
1.02
1.02
1.02
1.33
1.05
1.18
1.01
0.91
0.99
(Ho/Yb)N
1.32
1.37
1.38
1.18
1.30
1.39
0.66
1.44
0.47
La/Sm
9.34
10.25
14.05
11.56
23.91
13.18
9.27
3.40
6.23
Y/Yb
12.73
12.86
12.89
10.43
10.56
12.38
7.84
11.97
6.69
JO
U
LREE
HREE
Rb
194
175
174
153
183
143
174
173
206
Ba
3120
2280
1748
803
1548
747
2485
7310
118
JOURNAL PRE-PROOF TLG-14
NO.
TLG-15
TLG-16
XFG-61
Biotite monzogranite porphyry
LJG-03
LJG-04
HY-01
Grante pegmatite
HY-02
HY-03
Granodiorite
27.3
25.2
63.4
21.6
21.3
42.5
18.05
3.63
24.5
U
3.22
2.59
3.34
0.77
0.45
0.84
4.85
1.56
14.4
K
36692
38186
38020
42005
53045
39016
37688
90069
32873
Ta
1.49
1.29
2.37
0.60
0.10
0.20
1.20
0.70
2.10
Nb
27.6
25.2
35.1
19.4
2.60
5.70
21.4
29.6
39.2
Sr
850
480
567
258
265
402
786
997
142
P
1266
1440
655
218
131
87
43.6
43.6
43.6
Zr
898
996
574
169
96.0
212
82.0
37.0
86.0
5.70
2.70
1.10
4.80
6.61
1.23
3.53
0.61
O
F
Th
19.6
21.5
13.9
5.00
2.50
15.8
15.8
17.7
2.89
2.99
Ti
5575
5935
3417
899
659
659
300
360
180
Cr
38.0
22.0
16.0
16.0
32.0
10.0
9.00
31.0
9.00
Ni
5.10
5.40
2.80
2.90
3.00
2.10
1.60
1.70
1.30
V
78.0
86.0
49.0
8.00
6.00
11.0
8.00
32.0
2.00
Ga
27.6
26.8
25.9
19.1
15.7
22.2
17.6
19.0
26.3
PR
E-
PR
O
Hf Sm
Table 3. Whole-rocks Rb–Sr and Sm–Nd isotopic compositions of granitic rocks in the giant Huayangchuan ore district. Sr
87Rb/86Sr
87Sr/86Sr
2σ
(87Sr/86Sr)i
Sm
Nd
147Sm/144Nd
143Nd/144Nd
2σ
(143Nd/144Nd)i
εNd(t)
fSm/Nd
4
904
0.006530
0.710008
0.000012
0.7100
5.34
36.0
0.089657
0.511712
0.000006
0.511572
-17.5
-0.54
4
855
0.005872
0.709844
0.000010
0.7098
4.48
29.6
0.091480
0.511669
0.000005
0.511589
-17.2
-0.53
8
935
0.005184
0.709784
0.000009
0.7098
5.31
35.4
0.090663
0.511668
0.000005
0.511590
-17.1
-0.54
1
932
0.005605
0.709875
0.000010
0.7099
5.28
33.1
0.096415
0.511675
0.000005
0.511591
-17.1
-0.51
4
786
0.006388
0.707682
0.000008
0.7077
1.23
6.60
0.112650
0.511970
0.000005
0.511798
-10.5
-0.43
3
997
0.005022
0.706236
0.000010
0.7062
3.53
14.7
0.145164
0.512259
0.000004
0.512038
-5.9
-0.26
6
142
0.042130
0.717851
0.000010
0.7177
0.61
2.80
0.131688
0.512012
0.000006
0.511811
-10.3
-0.33
3
258
0.017162
0.759095
0.000012
0.7586
2.89
20.5
0.085196
0.511058
0.000005
0.510045
-5.0
-0.57
3
265
0.019984
0.758527
0.000010
0.7580
2.99
30.7
0.058853
0.510652
0.000005
0.509953
-6.8
-0.70
3
402
0.010294
0.731005
0.000009
0.7307
6.61
52.9
0.075511
0.510938
0.000005
0.510041
-5.1
-0.62
4
850
0.006588
0.722726
0.000010
0.7226
15.8
107
0.089404
0.511004
0.000004
0.509941
-7.0
-0.55
480
0.010551
0.718197
0.000010
0.7179
15.8
113
0.084605
0.510952
0.000006
0.509945
-6.9
-0.57
567
0.008855
0.717815
0.000011
0.7176
17.7
134
0.079716
0.510882
0.000005
0.509934
-7.1
-0.59
4
R N
U
JO
5
AL
b
Tab. 4. Zircon Lu–Hf isotopic compositions of granitic rocks in the giant Huayangchuan ore district. No.
T(Ma)
176Yb/177Hf
2σ
176Lu/177Hf
2σ
176Hf/177Hf
2σ
(176Hf/177Hf)i
0.000207
0.000528
0.000006
0.281486
0.000009
0.281468
Biotite monzoranite porphyry TLG-14-01
1808
0.026696
176Yb/177Hf
2σ
176Lu/177Hf
2σ
176Hf/177Hf
2σ
(176Hf/177Hf)i
TLG-14-02
1808
0.048930
0.000147
0.000965
0.000006
0.281589
0.000011
0.281556
TLG-14-03
1808
0.044731
0.000121
0.000844
0.000003
0.281507
0.000010
0.281478
TLG-14-04
1808
0.058169
0.000075
0.001121
0.000002
0.281506
0.000009
0.281468
TLG-14-05
1808
0.042489
0.001007
0.000820
0.000015
0.281556
0.000011
0.281527
TLG-14-06
1808
0.060825
0.000440
0.001102
0.000004
0.281553
0.000011
0.281515
TLG-14-07
1808
0.065562
0.000198
0.001215
0.000002
0.281514
0.000010
0.281472
TLG-14-08
1808
0.088290
0.001101
0.001564
0.000013
0.281493
0.000011
0.281439
TLG-14-09
1808
0.048719
0.000306
0.000959
0.000001
0.281556
0.000011
0.281523
TLG-14-10
1808
0.067081
0.000164
0.001266
0.000003
0.281467
0.000010
0.281423
TLG-14-11
1808
0.066550
0.000426
0.001227
0.000006
0.281520
0.000011
0.281478
TLG-14-12
1808
0.030207
0.000354
0.000609
0.000003
0.281508
0.000011
0.281487
TLG-14-13
1808
0.046892
0.000339
0.000935
0.000007
0.281465
0.000010
0.281433
TLG-14-14
1808
0.056432
0.000225
0.001124
0.000009
0.281463
0.000010
0.281425
TLG-14-15
1808
0.028021
0.000196
0.000560
0.000001
0.281434
0.000010
0.281414
TLG-14-16
1808
0.038190
0.000135
0.000779
0.000005
0.281477
0.000011
0.281450
TLG-14-17
1808
0.070990
0.000107
0.001359
0.000004
0.281502
0.000011
0.281456
TLG-14-18
1808
0.082321
0.000274
0.001496
0.000003
0.281471
0.000011
0.281420
TLG-14-19
1808
0.023253
0.000121
0.000448
0.000001
0.281474
0.000009
0.281458
TLG-14-20
1808
0.062662
0.000336
0.001266
0.000010
0.281503
0.000011
0.281460
TLG-14-21
1808
0.041184
0.000770
0.000759
0.000011
0.281503
0.000009
0.281477
TLG-14-22
1808
0.042288
0.000049
0.000873
0.000002
0.281512
0.000014
0.281482
TLG-14-23
1808
0.043672
0.000592
0.000869
0.000014
0.281430
0.000011
0.281400
TLG-14-26
1808
0.033521
0.000370
0.000638
0.000004
0.281499
0.000010
0.281477
TLG-14-27
1808
0.029192
0.000155
0.000585
0.000001
0.281481
0.000011
0.281461
1808
0.051517
0.000419
0.000992
0.000004
0.281464
0.000009
0.281430
1808
0.059278
0.000264
0.001157
0.000008
0.281507
0.000010
0.281467
1808
0.030307
0.000149
0.000596
0.000001
0.281428
0.000010
0.281407
1808
0.027043
0.000501
0.000799
0.000012
0.281488
0.000016
0.281460
XFG-61-01
1807
0.047304
0.000327
0.001108
0.000009
0.281473
0.000011
0.281435
XFG-61-02
1807
0.021910
0.000029
0.000489
0.000001
0.281474
0.000008
0.281458
XFG-61-03
1807
0.046635
0.000131
0.001098
0.000001
0.281478
0.000010
0.281440
XFG-61-04
1807
0.044459
0.000158
0.001002
0.000006
0.281484
0.000011
0.281450
XFG-61-05
1807
0.026697
0.000251
0.000609
0.000004
0.281482
0.000011
0.281461
XFG-61-10
1807
0.067429
0.000094
0.001517
0.000004
0.281461
0.000011
0.281409
XFG-61-11
1807
0.031379
0.000127
0.000728
0.000004
0.281493
0.000010
0.281468
XFG-61-13
1807
0.074256
0.000311
0.001690
0.000012
0.281481
0.000012
0.281423
XFG-61-15
1807
0.045536
0.000343
0.000970
0.000010
0.281501
0.000008
0.281468
XFG-61-16
1807
0.040336
0.000586
0.000907
0.000016
0.281504
0.000009
0.281473
XFG-61-19
1807
0.054649
0.000549
0.001222
0.000015
0.281483
0.000007
0.281441
XFG-61-20
1807
0.050290
0.000458
0.001143
0.000013
0.281488
0.000008
0.281449
XFG-61-27
1807
0.028635
0.000213
0.000654
0.000006
0.281452
0.000007
0.281430
XFG-61-26
1807
0.038665
0.000098
0.000859
0.000003
0.281502
0.000008
0.281473
TLG-14-28 TLG-14-30
R N
TLG-14-31 TLG-14-32
O
PR
E-
PR
AL
No.
F
T(Ma)
O
JOURNAL PRE-PROOF
JO
U
Granite pegmatite
T(Ma)
176Yb/177Hf
2σ
176Lu/177Hf
2σ
176Hf/177Hf
2σ
(176Hf/177Hf)i
1807
0.040083
0.000104
0.000877
0.000003
0.281419
0.000008
0.281389
HY-01-01
233.3
0.083813
0.000697
0.002103
0.000009
0.282208
0.000008
0.282199
HY-01-03
233.3
0.106369
0.000407
0.002489
0.000010
0.282248
0.000010
0.282237
HY-01-07
233.3
0.080769
0.000915
0.001891
0.000011
0.282297
0.000009
0.282288
HY-01-08
233.3
0.107863
0.000636
0.002192
0.000008
0.281433
0.000013
0.281423
HY-01-10
233.3
0.073364
0.000359
0.001816
0.000012
0.282246
0.000009
0.282238
HY-01-11
233.3
0.045265
0.000846
0.000905
0.000016
0.281452
0.000009
0.281448
HY-01-13
233.3
0.129510
0.002863
0.003230
0.000074
0.282253
0.000015
0.282239
HY-01-14
233.3
0.078528
0.000247
0.002285
0.000009
0.282247
0.000013
0.282237
HY-01-18
233.3
0.098963
0.001486
0.002756
0.000029
0.282292
0.000009
0.282280
HY-01-21
233.3
0.115516
0.000758
0.003393
0.000037
0.282226
0.000012
0.282211
HY-01-24
233.3
0.082470
0.000886
0.001979
O
JOURNAL PRE-PROOF
0.000023
0.282274
0.000009
0.282265
HY-01-25
233.3
0.075510
0.000384
0.001985
0.000007
0.282290
0.000010
0.282282
HY-01-28
233.3
0.077053
0.000432
0.002325
0.000011
0.282282
0.000012
0.282271
HY-01-30
233.3
0.095211
0.001019
0.002670
0.000031
0.282275
0.000010
0.282263
HY-01-31
233.3
0.071545
0.000241
0.001731
0.000005
0.282220
0.000009
0.282213
HY-01-32
233.3
0.109937
0.000419
0.002494
0.000007
0.282295
0.000010
0.282284
No. XFG-61-28
O
PR
E-
PR
Biotite monzogranite
F
Granodiorite
132.3
0.053807
0.000783
0.001300
0.000021
0.282158
0.000009
0.282154
HYC-12-02
132.3
0.051532
0.000177
0.001318
0.000005
0.282047
0.000010
0.282044
HYC-12-03
132.3
0.031961
0.000293
0.000738
0.000007
0.282280
0.000009
0.282278
HYC-12-04
132.3
0.059660
0.000192
0.001529
0.000014
0.282188
0.000008
0.282185
HYC-12-05
132.3
0.033454
0.000275
0.000835
0.000006
0.282148
0.000008
0.282146
132.3
0.055091
0.000320
0.001409
0.000005
0.282154
0.000009
0.282150
132.3
0.032486
0.000510
0.000964
0.000019
0.281977
0.000011
0.281975
132.3
0.044486
0.000453
0.000945
0.000009
0.282261
0.000009
0.282259
HYC-12-09
132.3
0.018309
0.000124
0.000528
0.000004
0.281997
0.000008
0.281996
HYC-12-10
132.3
0.035196
0.000394
0.000862
0.000009
0.282133
0.000008
0.282131
HYC-12-11
132.3
0.025927
0.000068
0.000670
0.000002
0.281820
0.000008
0.281818
HYC-12-13
132.3
0.063024
0.000444
0.001973
0.000016
0.282161
0.000008
0.282157
HYC-12-14
132.3
0.045999
0.000181
0.001253
0.000007
0.282052
0.000008
0.282049
HYC-12-15
132.3
0.052236
0.000536
0.001133
0.000010
0.282275
0.000010
0.282272
HYC-12-16
132.3
0.042728
0.000228
0.001077
0.000005
0.282078
0.000007
0.282075
HYC-12-17
132.3
0.036000
0.000462
0.000837
0.000009
0.282114
0.000008
0.282112
HYC-12-18
132.3
0.041567
0.001017
0.001274
0.000034
0.281832
0.000009
0.281829
HYC-12-19
132.3
0.031240
0.000177
0.000835
0.000003
0.282023
0.000010
0.282021
HYC-12-21
132.3
0.027084
0.000045
0.000772
0.000002
0.282200
0.000008
0.282198
HYC-12-22
132.3
0.046977
0.000672
0.001651
0.000037
0.282042
0.000009
0.282038
HYC-12-23
132.3
0.047741
0.000600
0.001208
0.000010
0.282093
0.000008
0.282090
HYC-12-24
132.3
0.040395
0.000191
0.000978
0.000004
0.282087
0.000008
0.282084
HYC-12-25
132.3
0.034548
0.000448
0.000876
0.000007
0.282132
0.000008
0.282130
HYC-12-26
132.3
0.083433
0.000468
0.002364
0.000012
0.282109
0.000013
0.282103
HYC-12-06 HYC-12-07
JO
U
R N
HYC-12-08
AL
HYC-12-01
JOURNAL PRE-PROOF
No.
176Yb/177Hf
2σ
176Lu/177Hf
2σ
176Hf/177Hf
2σ
(176Hf/177Hf)i
132.3
0.037929
0.000108
0.000848
0.000001
0.282167
0.000008
0.282165
R N
AL
PR
E-
PR
O
O
F
HYC-12-27
T(Ma)
Highlights
U
(1) The Huayangchuan granitic rocks dated at ca. 1.8 Ga, ca. 233 Ma and ca. 132 Ma.
JO
(2) The granite pegmatite is locally associated with the Huayangchuan uranium
mineralization. (3) The
granodiorite is consistent with the main mineralization of the Huayangchuan deposit.
(4) The Huayangchuan granitic rocks are mainly sourced from the Taihua Group.