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Article

Origin of Mesozoic Porphyritic Rocks and Regional Magmatic Evolution in the Zijinshan Ore Field of Fujian Province, China: Hf-O Isotope Characteristics of Magmatic Zircons

by
Wenhui Zhang
1,*,
Liyuan Wang
1,*,
Xupeng Lv
2,
Xiaomin Li
1,
Shuaiqi Yan
1 and
Juntao Nie
1
1
College of Zijin Mining, Fuzhou University, Fuzhou 350108, China
2
Yunnan Institute of Geological Survey, Kunming 650000, China
*
Authors to whom correspondence should be addressed.
Minerals 2020, 10(12), 1143; https://doi.org/10.3390/min10121143
Submission received: 15 November 2020 / Revised: 14 December 2020 / Accepted: 17 December 2020 / Published: 20 December 2020
(This article belongs to the Special Issue Magma Ascent and Evolution: Insights from Petrology and Geochemistry)
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Abstract

:
Mesozoic porphyritic rocks from the Zijinshan area, southwestern Fujian Province, China, are andesitic to rhyolitic in composition. The whole-rock SiO2 contents of these rocks are between 62.5% and 78.1%. Magmatic zircon from the Mesozoic porphyritic rocks was determined via secondary-ionization mass spectrometry (SIMS) for the U-Pb age and Hf and O isotopes. The zircon U-Pb ages could be mainly divided into three age groups: Group 1: ~138.8 Ma; Group 2: 109.2~107.4 Ma; and Group 3: 99.7~98.2 Ma. The εHf(t) and δ18O values of the porphyritic zircons showed that the porphyritic rocks in Group 2 were more affected by mantle-derived magma. Combined with previous research results, the medium-acidic magmatism in the southwestern Fujian Province can be divided into eight periods: Paleoproterozoic, Mesoproterozoic, Middle Neoproterozoic, Silurian to Lower Devonian, Permian to Triassic, Middle Jurassic to early Lower Cretaceous, late Lower Cretaceous, and late Lower Cretaceous to early Upper Cretaceous. The Paleoproterozoic crust was the predominant magmatic source for the subsequent Mesoproterozoic to Jurassic magmatism, but the only melts that were closely related to mineralization were derived from partial melting of the Mesoproterozoic crust and a more depleted upper mantle.

1. Introduction

The Zijinshan ore field, the largest porphyry-epithermal mineralization system in southeast China, is located in the southwestern Fujian Province (Figure 1) [1,2]. The major economic deposits in the region include: (1) the Zijinshan high-sulfidation epithermal deposit [3,4,5], (2) the Luoboling Cu-Mo-Au porphyritic deposit [6], (3) the Yueyang low-sulfidation epithermal Ag polymetallic deposit [7], and (4) the Wuziqilong transitional Cu deposit [8,9]. Zijinshan mineralization was closely related to two large-scale intermediate-acid magmatic activities in the Mesozoic: late Jurassic (165–149 Ma) and Cretaceous (118–92 Ma) [10,11,12,13,14]. The late Jurassic intrusive rocks were mainly composed of medium-to coarse-grained monzogranite and granite, and the early Cretaceous intrusive-volcanic rocks were mainly hypabyssal intrusive rock or subvolcanic porphyries such as granodioritic porphyry, granitic porphyry, quartz porphyry, and dacitic porphyry. The dacitic and/or granodioritic porphyries were strongly associated with the Zijinshan Cu–Au deposit and the Luoboling porphyry Cu-Mo mineralization [15,16].
As Cretaceous porphyritic rocks play an important role in mineralization, much attention has been paid to their genesis [14,17]. However, as the magmatic rocks in the Zijinshan area were usually subjected to intense alteration, it is difficult to completely describe the characteristics of the original magma from a whole-rock geochemical study. Even though zircon Hf isotopes have been conventionally used to study the origin of these rocks [4,10], the large range of Hf isotopic compositions from various mantle sources sometimes prevents the effective identification of the magmatic source and, thus, the genesis of the economic ore deposits.
In addition to U, Pb, and Hf isotopes, zircon has a high closure temperature for oxygen. Oxygen isotopes retain their original basic oxygen isotope characteristics even during high-grade eclogite-facies metamorphism and, therefore, work as more effective indicators for magma genesis [18]. Studies of oxygen isotopes in magmatic zircons have shown that mantle-derived zircons have almost uniform δ18O values (5.3 ± 0.6‰) [19,20]. Increasing δ18O values generally indicate the involvement of crustal materials in a magmatic source. Therefore, the oxygen isotopic signatures of magmatic zircons can provide robust indicators of the interaction between crust and mantle in a given region [21,22,23,24].
In this study, we focus on Mesozoic porphyritic rocks in the Zijinshan area, as these rocks are closely related to the formation of economic ore deposits. The zircon Hf-O isotopic data of the porphyritic rocks demonstrated that the mantle-derived materials contributed more to the early Cretaceous melts than the late Cretaceous ones. The Jurassic porphyritic rocks showed more involvement in crustal materials. We also discuss the magmatic evolution of the crustal source from Proterozoic to Mesozoic.

2. Geological Background and Petrography

2.1. Geological Background

The Zijinshan area is located in the southwestern Fujian Provence (Figure 1b), China (Figure 1a). The northwest-striking Yunxiao-Shanghang fault zone and several northeast-orienting Xuanhe anticlinoria are the chief ore-controlling structures. Flysch sediments metamorphosed by the Sinian and early Paleozoic periods are outcropped in the Zijinshan area (Figure 1c). The Indosinian orogeny, which occurred in the eastern part of China during the early Triassic, resulted in a change in the tectonic framework in Southeast China from the predominantly Tethys tectonic domain to the circum Pacific active continental margin [25,26,27,28]. The orogeny formed a series of intermediate-acid igneous rocks accompanied by large-scale mineralization [25].
The Cretaceous (105 Ma) granodioritic porphyry invaded and was extensively buried at the depth of this area, which was not only associated with the Zhongliao porphyry copper (molybdenum) deposit but also provided a heat source for the epigenetic hydrothermal Cu-Au deposits that resulted in large-scale Cu–Au mineralization [29,30,31,32,33]. However, the dacitic porphyry contributed to the Zijinshan Cu–Au deposit, while the granodioritic porphyry contributed to the Luoboling Cu-Mo ore [34].

2.2. Petrography

Nine samples were collected for studies of bulk-rock chemistry and U-Pb, Hf, and O isotopes of zircon. Microscopic photographs of representative samples are shown in Figure 2. The porphyritic rocks in the region were found to be mainly granitic porphyry, with a minor amount of granodioritic porphyry (sampe CX-5). The granitic porphyry had a porphyritic texture (Figure 2a,b), with the matrix of a microcrystalline–cryptocrystalline texture (Figure 2d). We found that some materials of the matrix were devitrified (Figure 2c). The content of phenocrysts was found to be about 20–30%, mainly composed of alkali feldspar, plagioclase, quartz, and a small amount of biotite and amphibole. The alkali feldspar was in the shape of a euhedral–subhedral plate, exhibiting common kaolinization and, to a lesser degree, sericitization. The quartz was granular and normally eroded. Some quartz grains underwent late hydrothermal carbonate alteration (Figure 2e). The biotite was generally chloritized with an abnormal interference color (Figure 2d,h). The amphiboles were also strongly altered by carbonation and chloritization (Figure 2f). Sericitization was common in the plagioclase (Figure 2n). The granodioritic porphyry had a porphyritic structure with some phenocrysts fragmented and cut through by the late quartz veins (Figure 2k). The fine-grained matrix consisted of long strips of plagioclase that were arranged roughly in orientation.

3. Analytical Methods

3.1. Major and Trace Element Analysis

Whole-rock samples were analyzed for major and trace elements at the Institute of Regional Geology and Mineral Resources Survey in Hebei Province, China. The major elements were analyzed using the X-ray fluorescence (XRF) method with an analytical error of <2%. Rare earth and other trace elements were analyzed by using plasma mass spectrometry (ICP-MS) with an analytical error of <5%.

3.2. Zircon U-Pb Dating

Zircons from about 20 kg of the sample were first separated using magnetic and heavy liquid separation methods, and then it was hand-picked under a binocular microscope. Zircon grains and a standard sample (Qinghu, Plésovice and 91500) were stuck onto the target using epoxy resin, and gold was sprayed on the surface after polishing the internal zircon. The morphology and internal structure of the zircons were studied using the cathodoluminescence (CL) technique with a JXA-8100 Electron Probe Microanalyzer for high-resolution imaging and spectroscopy at the State Key Laboratory of Continental Tectonics and Dynamics in Chinese Academy of Geological Sciences. The zircon in-situ O isotopic ratios were analyzed first, and the U-Pb and Hf isotope were subsequently analyzed at the same point.
Zircon U-Pb and Pb-Pb dating were conducted using a Cameca IMS 1280 ion microprobe (secondary-ionization mass spectrometry (SIMS)) at the Institute of Geology and Geophysics, Chinese Academy of Sciences (CAS) in Beijing. The detailed method of the analysis can be found in [18]. A single O2− ion beam (20 × 30 µm in size with 10 nA of strength) bombarded the sample surface with an acceleration voltage of −13 kV. Oxygen flow increased the sample chamber pressure to approximately 5 × 10−6 T in order to improve the sensitivity of the Pb+ ion in zircon. Seven sets of data were analyzed for each sample spot, and the measuring time was approximately 12 min. The obtained standard deviation of 1.5% (1σ) through long-term monitoring of the standard sample [34] and the internal test accuracy of single sample points together determined the single point error. Standard zircon 91500 (1065 Ma) was used to correct the Pb/U ratios and calculate the Th and U contents of the zircon samples (Th = 29 μg/g; U = 81 μg/g) [35]. Ordinary Pb was corrected by measuring 204Pb. The analysis error of the isotope ratio and age for a single point was 1σ. The data were processed using the ISOPLOT software [36].

3.3. O Isotope Analysis

Zircon in-situ O isotopes were also analyzed by using the Cameca IMS 1280 ion microprobe (CASIMS) at the Institute of Geology and Geophysics at the CAS. A detailed analysis method can be found in [37]. A single 133Cs+ ion beam with a strength of 2 nA bombarded the sample surface and then received both 16O and 18O at the same time via two Faraday cups. The single-point measurement time was approximately 5 min, and the accuracy of the single group 18O/16O data were generally better than 0.2‰–0.3‰ (1σ). The external precision of the sample was 0.5‰ (2SD). The quality fractionation of the instrument was corrected by the Penglai zircon standard [34]. The measured 18O/16O ratio was corrected using the Vienna standard mean ocean water (V-SMOW) value (18O/16O=0.0020052). In this study, (δ18O)M = ((18O/16O)M/0.0020052 − 1) × 1000(‰), instrumental mass fractionation (IMF) = (δ18O)M(standard) − (δ18O)VSMOW, δ18Osample = (δ18O)M + IMF.

3.4. Hf Isotope Analysis

In-situ zircon Lu-Hf isotopic measurements were performed on a Neptune Plus Multi Collector -ICP-MS, coupled with a 193 nm resolution laser ablation system at the Institute of Geology and Geophysics at the CAS. A detailed description of analytical methods can be found in [38]. The time of laser ablation was 26 s. The laser ablation pulse frequency was 10 Hz, and the pulse power was 100 mJ, with a beam spot size of approximately 60 µm. The isobaric interference of 176Lu and 176Yb to 176Hf was rectified by monitoring the signal strength of 175Lu and 172Yb using the 175Lu/176Lu ratio (0.02655) and the 176Yb/172Yb ratio (0.5886), respectively [39]. Standard zircon 91500 crossing with zircon sample analysis was used for the external monitoring of instrument drift. In the process of the analysis, the average 176Hf/177Hf ratio for the zircon standard Mud Tank was 0.282491 ± 27 (2σ), and it was 0.281971 ± 26 (2σ) for GJ, which was consistent with the results of the literature within the error range [40]. The ƐHf value and two phase model calculation age were calculated according to [38] and the references therein using (176Lu/177Hf)CHUR = 0.0332; (176Hf/177Hf)CHUR,0 = 0.28277; (176Lu/177Hf)DM = 0.0384; and (176Hf/177Hf)DM = 0.28325. The fcc, fs, and fDM represent the fLu/Hf of the continental crust, samples, and depleted mantle, respectively. T is the age of sample formation. Λ = 1.867 × 10−11 year−1.

4. Results

4.1. Zircon SIMS U/Pb Age

The analyzed zircons were mostly colorless and transparent crystals, ranging from semi-automorphic to idiomorphic, with a length of 100–400 μm and varying length/width ratio from 1:1 to 4:1. The CL images clearly showed that the internal structure of the zircons was oscillatory zoning (Figure 3). No influence of alteration on these zircon grains was observed. The Th/U ratios of the zircons were generally >0.1 (Supplementary Table S1), which is typical of magmatic zircons [41].
The detailed dating results are listed in Supplementary Table S1. Because of errors in counting statistics during the analysis, the 207Pb/206Pb ages were more accurate for older (>1 Ga) zircons, whereas the 206Pb/238U ages were more accurate for younger zircons [42]. Therefore, we use the 206Pb/238U ages for younger zircons in the following discussion.
Fifteen analyses on zircon grains from sample CX-9 yielded concordant 206Pb/238U dates ranging from 136.9 ± 2.0 to 141.2 ± 2.1 Ma with a weighted mean age of 138.8 ± 1.1 Ma (MSWD = 15; Figure 4). Zircon samples from EMG-1, PD-390, and CX-5 displayed a weighted mean age in the range of 109.2–107.4 Ma. They yielded concordant 206Pb/238U dates ranging from 103.7 ± 1.6 to 118.2 ± 1.4 Ma, except for one (EMG-1@13) that was 153.0 ± 2.3 Ma. Zircon samples from SF-4, CX-2, CX-4, SMS-1, and SMS-2 displayed a weighted mean age in the range of 99.7–98.2 Ma, with concordant 206Pb/238U dates ranging from 103.9 ± 1.5 to 96.5 ±1.5 Ma. Two xenocrystic zircons had ages of 224.8.0 ± 3.3 Ma (SF-4@13) and 755.6 ± 10.7 (SMS-2@13).
Excluding ages from the xenocrystic zircons, the ages were divided into three groups: Group 1: ~138.8 Ma; Group 2: 109.2–107.4 Ma; and Group 3: 99.7–98.2 Ma.

4.2. Characteristics of Major and Trace Elements

The whole-rock SiO2 contents of the sample ranged from 62.46 to 78.09%. The relatively high SiO2 contents are usually combined with low Fe2O3T, MgO, and CaO (Supplementary Table S2). The porphyry were characterized by low-to-high concentrations of Na2O between 0.09% and 4.27%, high K2O and Na2O between 4.24% and 8.98%, MgO of 0.1–3.6 % with most lower than 1%, and Al2O3 between 11.63 and 15.92%. In the SiO2 versus K2O and Na2O diagram, most samples plotted in the granite and granodiorite fields (Figure 5a). They had high K2O contents (3.27–8.85%), and all samples were located in the subalkaline and high-K calc-alkaline fields (Figure 5b). The aluminum saturation index values (A/CNK) varied from 0.95 to 3.26, indicating metaluminous-to-strongly peraluminous characteristics.
Most samples were enriched in light rare earth elements (LREEs) and moderately depleted in heavy rare earth elements(HREEs), with total amounts of 146.3–215.6 ppm. In the chondrite-normalized rare earth element (REE) patterns (Figure 5c), all samples showed obvious enrichment in LREEs ((La/Yb)N = 6.32–30.71) with moderately negative Eu anomalies (Eu/Eu* = 0.21–0.94). Such REE patterns reflected feldspar fractional crystallization or poorly soluble residuum in the early stage of magmatism. The contents of the HREEs decreased with age, with sample CX-9 (age = 138.8 ± 1.1 Ma) showing the highest contents of Yb and Lu (7.13 and 1.15 ppm, respectively) and the CX-2 (age = 99.56 ± 0.86 Ma) showing the lowest (1.04 and 0.24 ppm, respectively). Strongly negative Eu anomalies could be observed in samples CX-9 and SMS-1, indicating that they may have been formed in low oxygen fugacity and consequently experienced the significant crystallization of plagioclase in the magma source area.
The trace element abundance diagrams of the porphyritic rocks display roughly similar patterns with negative anomalies of Ba, Nb, Sr, P, and Ti anomalies combined with small positive Rb, Th, U, La, Ce, Nd, and Hf anomalies (Figure 5d). The enrichment in LILEs and depletion in HFSEs in the porphyry samples indicate the influence of fluids in subduction conditions. The significant negative Ba anomalies are thought to be the result of alkali feldspar-dominated fractionation. Positive Rb and negative Sr anomalies, both of which are associated with negative Eu anomalies, are consistent with dominant plagioclase fractionation. The significant Ti depletions were due to magnetite and ilmenite fractionation.
As the alteration of the Mesozoic granite samples in the Zijinshan area is strong, its major and trace elements may not be reliably used to describe the characteristics of the source region.

4.3. O-Isotope Composition of Zircons

The zircon oxygen isotopic data are listed in Supplementary Table S3 and shown in Figure 6. The δ18O values of the Group 1 (~138.8 Ma) zircons ranged from 6.96 to 8.17‰, and those of Group 2 (109.2–107.4 Ma) ranged from 5.54 to 7.72‰. The δ18O values of the Group 3 (99.7–98.2 Ma) zircons ranged from 6.34 to 7.62‰, with one showing an extremely high value (δ18O = 9.02 of SF-4@11). Additionally, two inherited zircon grains from the EMG-1 and SF-4 (153.0 and 224.8 Ma) showed extremely high δ18O values (9.27 and 10.45‰, respectively).

4.4. Hf-Isotope Compositions of Zircons

Lu-Hf isotopic ratios were determined on the same or similar domains as the zircon grains analyzed for U-Pb and O isotopes. The analytical results are listed in Supplementary Table S3 and shown in Figure 7. The εHf(t) values were calculated using their U-Pb ages. The εHf(t) values of Group 1 zircons ranged from −6.1 to −15.3, and those for Group 2 ranged from 1.6 to −5.3. The εHf values of Group 3 zircons ranged from 0.0 to −7.5, with two grains having extremely low εHf(t) values. Zircon SF-4@11 had a low εHf(t) of −12.5, with a high δ18O‰ of 9.02, whereas zircon SMS-1@9 had an even lower εHf(t) of −20.4, with a normal δ18O value (δ18O‰ = 6.34).

5. Discussion

5.1. Magmatic Source

Zircon has high closure temperatures for U, Pb, O, and Hf; thus, it is less susceptible to mixing the overlying crustal material during magma ascent. Therefore, these isotopic signatures could represent the geochemical characteristics of the original magma.
As discussed before, the ages of the Zijinshan porphyritic rocks were divided into three groups: Group 1: ~138.8 Ma; Group 2: 109.2–107.4 Ma; and Group 3: 99.7–98.2 Ma. In Group 1, the zircon δ18O values of sample CX-9 ranged from 6.96 to 8.17‰ (Figure 6), which was higher than the primitive mantle value (5.3 ± 0.3‰) [19,20]. Meanwhile, the εHf(t) values of the Group 1 zircon ranged from −6.1 to −15.3 (Figure 7). The relatively high δ18O and low εHf(t) values suggest that crustal material played an important part in magma genesis. The fact that the Hf two-episode depleted mantle model ages (TDM2) of the Group 1 zircons were mainly in the range of 1576–1818 Ma (except one in 2156 Ma) implies the presence of a late Proterozoic crustal source for the Group 1 porphyritic rocks (Supplementary Table S3; Figure 8).
The δ18O values of the Group 2 zircons ranged from 5.54‰ to 7.72‰, which were closer to the mantle value when compared to the other zircons groups. The εHf(t) values of the zircons ranged from 1.6 to −5.3, which belonged to the region between the depleted mantle and mafic crust. The low δ18O and high εHf(t) values reflected a higher proportion of mantle material contributing to the acidic magma. The Group 2 zircons had Hf TDM2 ages that were mainly in the range of 1066–1535 Ma (except two zircons aged at 1759 Ma), indicating the presence, among the others, of a Middle Proterozoic crustal source (Figure 8). Magmatic emplacement in this period probably resulted from the upwelling of the asthenosphere.
The δ18O values of the Group 3 zircons ranged from 6.34‰ to 7.62‰, with one having an extremely high value (δ18O = 9.02 of SF-4@11). The εHf values ranged from 0.0 to −7.5, with two extremely low εHf(t) values. One zircon grain (SF-4@11) had a calculated εHf(t) of −12.5, associated with a high δ18O value (δ18O = 9.02‰). Another grain (SMS-1@9) had the lowest εHf(t) of −20.4, but with a normal δ18O value (δ18O = 6.34‰). Most zircons had Hf TDM2 ages of 1400–1700 Ma (Figure 8). Therefore, it is possible that the Group 3 rocks had a mixed source composed of Group 1 and Group 2 rocks. In Group 3, the influence of mantle-derived magma was less than that in Group 2, and there was an increasing tendency indication of the crustal source. The δ18O and εHf(t) values also showed the mixing characteristic of Group 1 and Group 2 magma.
In summary, Group 2 was more affected by mantle-derived magmas. This conclusion is consistent with previous studies arguing that the late Early Cretaceous was an important ore-forming period, and some ore-forming elements were derived directly from the mantle. It has been widely accepted that Cretaceous magmatic rocks formed in an extensional tectonic setting and are probably related to subduction of the Western Pacific plate [4,14].

5.2. Regional Magmatic Evolution

Combined with the previous data of the SIMS U-Pb age of magmatic zircons, it can be summarized that the magmatic activities in the southwestern Fujian Province can be divided into eight main periods. The zircon O and Hf data indicated that the different episodes of magmatic rocks had different δ18O and εHf(t) signatures, reflecting different magma sources and tectonic environments [43,44]. Following is a summary of the magmatic zircons categorized by period. Some of them were captured by granite and mafic dikes, some samples were directly crystallized from intermediate-acid magmatic rocks, and the rest were sampled from the metamorphose basement of Precambrian.
1.
Paleoproterozoic (2467~1950 Ma)
Zircons of Early Proterozoic ages were collected from basaltic dikes [41]. The measured δ18O values (4.42–8.09‰; average 5.81‰) of these zircons were close to the δ18O value of the zircons crystallized from mantle-derived magmas [19]. The εHf(t) values of these zircons were mainly between 2.2 and −7.9, falling within the depleted mantle and average crust. The Hf two-stage depleted mantle model ages (TDM2) were mainly in the Archaeozoic (Figure 8). This indicated that the magmatism was derived from the partial melting of an ancient depleted mantle and an Archaeozoic crust.
2.
Mesoproterozoic (1514~933 Ma)
The Mesoproterozoic magmatic zircons from our study displayed a large variation both in Hf isotopic compositions (εHf(t) = from 4.5 to −15.5) and in oxygen isotopic compositions ranging from a lower than the normal mantle value of 3.79‰ to supracrustal component of 9.14‰. Most of the Mesoproterozoic zircons yielded Paleoproterozoic TDM2 ages (1.7–2.5 Ga). These characteristics implied that the Mesoproterozoic magmatism was generated mainly by the partial melting of the Paleoproterozoic crustal materials and mixed with depleted mantle-derived magmas.
3.
Middle Neoproterozoic (705~647 Ma)
Only five captured magmatic zircon grains were dated during this period. Their values of δ18O and εHf(t) varied in a limited range. This suggests that, from the Late Proterozoic to Pre-Silurian, there was probably no significant magmatism in this area.
4.
Silurian to Lower Devonian (443~395 Ma)
Zircons analyzed from this period showed relatively low εHf(t) values and plotted along the mafic crustal evolution line (Figure 8). The δ18O values of the zircons were higher than those of the others (Figure 7). The calculated Hf TDM2 ages were within the Paleoproterozoic (Figure 8). This suggested that magma mainly came from the partial melting of the Paleoproterozoic mafic crust and mantle materials had a smaller contribution.
5.
Permian to Triassic (277~211 Ma)
In this period, the εHf(t) and δ18O values of zircons varied over a wide range. This suggested magmatic mixing between the depleted mantle and mafic crust. However, the contribution of mantle material to magma was more significant than that of the previous Silurian magmas. The age of the crustal source was mainly Paleoproterozoic, with a minor contribution from the Middle Proterozoic crust.
6.
Middle Jurassic to Early Lower Cretaceous (174~137 Ma)
Late Jurassic granites were found to be widely distributed in the Zijinshan area. The magmatic zircons generally showed εHf(t) values of <0 and δ18O values of >6. Zircon Hf TDM2 ages were mainly from the Paleoproterozoic. This was the result of mixing of the mantle source material and the molten magma of the Paleoproterozoic crust.
7.
Late Lower Cretaceous (118~102 Ma)
Cretaceous shallow intrusive and volcanic rocks were found to be widely distributed in the Zijinshan area, with limited variations in εHf(t) and δ18O values. This indicated that the composition of the source region was relatively homogeneous. The low δ18O and high εHf(t) values suggested that the strongest mantle-derived magma intrusion occurred in this area in the Paleozoic. For all the magmatic activity in the region, only zircons from this period showed that the crustal component of the magma source was from the partial melting of the Middle Proterozoic strata, as shown by their Hf TDM2 ages (Figure 8). This period was an important Cu-Au-Ag mineralization period in the Zijinshan region. Both mantle-derived materials and materials derived from the Middle Proterozoic crust probably contributed to large-scale mineralization.
8.
Late Lower Cretaceous to Early Upper Cretaceous (101~92 Ma)
The compositional ranges of εHf(t) and δ18O values were also relatively limited similar to those observed in the late Early Cretaceous zircons. The limited variation of zircon εHf(t) and δ18O values in the Cretaceous felsic magmatism implied that the lower crust had been transformed into a more uniform lower crust. The zircon Hf TDM2 in this period, as well as εHf(t) and δ18O values, fell into the range between the Late Jurassic and Earliest Late Cretaceous.
In summary, the Paleoproterozoic crust was the main magmatic source for Mesoproterozoic to Jurassic magmatism (Figure 8). For pre-Mesoproterozoic magmatism (in period 1), crustal materials came from the partial melting of both the Archaeozoic and Paleoproterozoic crusts. Mantle-derived magmas played an important role in the formation of the Mesoproterozoic and earlier magmatism. From Mesoproterozoic to lower Devonian, the role of crustal melting in magmatic genesis gradually increased at the expense of the mantle component (Figure 7 and Figure 8). However, the contribution of mantle-derived materials increased in the magmatism from the Middle Jurassic to the late Lower Cretaceous (from period 6 to period 7). Intensive crust–mantle interactions may have caused a higher degree of the partial melting of the Mesoproterozoic crust. Mantle and Mesoproterozoic crustal materials provided sufficient ore-forming components and eventually led to the formation of large-scale deposits in the region. Period 8 was a continuation of Late Early Cretaceous magmatism. At this time, the mantle source invasion was reduced, the crust source became more homogeneous, and some mineralization continued.

6. Conclusions

(1) The ages of Mesozoic porphyritic rocks in the Zijinshan ore field region could be divided into three groups: Group 1: ~138.8 Ma; Group 2: ~109.2–107.4 Ma; and Group 3: ~99.7–98.2 Ma. Mantle-derived magma made a significant contribution to the Group 2 porphyries.
(2) Based on all the available SIMS U-Pb age data of the zircons, the medium-acidic magmatism in the southwestern Fujian province could be divided into eight periods: Paleoproterozoic, Mesoproterozoic, Middle Neoproterozoic, Silurian to Lower Devonian, Permian to Triassic, Middle Jurassic to Early Lower Cretaceous, Late Lower Cretaceous, and Late Lower Cretaceous to Early Upper Cretaceous.
(3) Paleoproterozoic crust was the main magmatic source for Mesoproterozoic to Jurassic magmatism, but only magmatism that was closely related to mineralization was derived from partial melting of the Mesoproterozoic crust and a more depleted mantle.
(4) Intensive crust–mantle interactions may have caused a higher degree of partial melting of the Mesoproterozoic crust. Mantle and Mesoproterozoic crustal materials provided sufficient ore-forming components and eventually led to the formation of large-scale deposits in the region.

Supplementary Materials

The following are available online at https://www.mdpi.com/2075-163X/10/12/1143/s1, Supplementary Table S1: U-Pb zircon dating results of the porphyritic rocks from the Zijinshan area; Table S2: Whole-rock geochemical data of the porphyritic rocks from the Zijinshan area; and Table S3: Hafnium and oxygen isotopes of the porphyritic rocks from the Zijinshan area.

Author Contributions

Conceptualization, W.Z. and L.W.; investigation, X.L. (Xiaomin Li); data curation, S.Y., J.N. and X.L. (Xupeng Lv); writing—original draft preparation; W.Z.; writing—review and editing; L.W. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by National Natural Science Foundation of China, grant number 41873012, 41903007.

Acknowledgments

We would like to thank Yue-Heng Yang for help in zircon analysis, Qiu-Li Li and other colleagues from IGGCAS for help in SIMS O analysis.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Geological sketch map of the China (a), Fujian Province (b), and the Zijinshan area (c).
Figure 1. Geological sketch map of the China (a), Fujian Province (b), and the Zijinshan area (c).
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Figure 2. Photographs showing micro-structures of the studied porphyry in the Zijingshan area. (a,b) granite porphyry with plagioclase and quartz phenocrysts; (c) felsic minerals matrix of the granitic porphyry developed devitrification phenomenon; (d) chloritization was developed along the cleavage fracture of biotite; (e) quartz phenocrysts of granitic porphyry were featured frequently with melting corrosion structure; (f) amphiboles were strongly altered with carbonation and chloritization; (g–k) granodioritic porphyry had a porphyritic structure, and plagioclase microcrystals were developed in the matrix; (i) quartz phenocrysts set in a fne- to micro-grained holocrystalline matrix; (m) quartz phenocryst with a typical recrystallized rim with micro-inclusions; (g–k) the matrix had a microcrystalline structure, and plagioclase was partially sericized; (n) biotite and plagioclase phenocrysts developed chloritization and sericization, respectively; and (o) plagioclase in the matrix had obvious sericization; abbreviations: Q: quartz; Pl: plagioclase; Kfs: K-feldspar; Bi: biotite; Amp: amphibole; Ser: Sericite; and Chl: chlorite.
Figure 2. Photographs showing micro-structures of the studied porphyry in the Zijingshan area. (a,b) granite porphyry with plagioclase and quartz phenocrysts; (c) felsic minerals matrix of the granitic porphyry developed devitrification phenomenon; (d) chloritization was developed along the cleavage fracture of biotite; (e) quartz phenocrysts of granitic porphyry were featured frequently with melting corrosion structure; (f) amphiboles were strongly altered with carbonation and chloritization; (g–k) granodioritic porphyry had a porphyritic structure, and plagioclase microcrystals were developed in the matrix; (i) quartz phenocrysts set in a fne- to micro-grained holocrystalline matrix; (m) quartz phenocryst with a typical recrystallized rim with micro-inclusions; (g–k) the matrix had a microcrystalline structure, and plagioclase was partially sericized; (n) biotite and plagioclase phenocrysts developed chloritization and sericization, respectively; and (o) plagioclase in the matrix had obvious sericization; abbreviations: Q: quartz; Pl: plagioclase; Kfs: K-feldspar; Bi: biotite; Amp: amphibole; Ser: Sericite; and Chl: chlorite.
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Figure 3. Zircon cathodoluminescence (CL) images of porphyritic rocks from the Zijinshan area. The white circle represents the analysis location of the Hf-O and U/Pb isotopes.
Figure 3. Zircon cathodoluminescence (CL) images of porphyritic rocks from the Zijinshan area. The white circle represents the analysis location of the Hf-O and U/Pb isotopes.
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Figure 4. U–Pb Concordia plots illustrating the U–Pb ages of porphyritic rocks from the Zijingshan area.
Figure 4. U–Pb Concordia plots illustrating the U–Pb ages of porphyritic rocks from the Zijingshan area.
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Figure 5. Geochemical classification diagrams of porphyritic rocks from the Zijingshan area. (a) TAS (Total Alkali vs. Silica) diagram; (b) K2O versus SiO2 diagram; (c) standardized rare earth element; and (d) incompatible trace element diagrams.
Figure 5. Geochemical classification diagrams of porphyritic rocks from the Zijingshan area. (a) TAS (Total Alkali vs. Silica) diagram; (b) K2O versus SiO2 diagram; (c) standardized rare earth element; and (d) incompatible trace element diagrams.
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Figure 6. Zircon δ18O versus magmatic zircons age from the Zijinshan ore field. δ18O value in mantle zircons = 5.3 ± 0.6 (2SD) [19]. Blue triangle represents Group 1, green box represents Group 2, red circles represent Group 3, and white circles represent other literature data. (a) oxygen isotopic characteristics of Zircons from the Jurassic to Cretaceous period; (b) oxygen isotopic characteristics of zircons from proterozoic to Cretaceous in the study area, note that Precambrian zircons show a negative correlation (increase in δ18O with time).
Figure 6. Zircon δ18O versus magmatic zircons age from the Zijinshan ore field. δ18O value in mantle zircons = 5.3 ± 0.6 (2SD) [19]. Blue triangle represents Group 1, green box represents Group 2, red circles represent Group 3, and white circles represent other literature data. (a) oxygen isotopic characteristics of Zircons from the Jurassic to Cretaceous period; (b) oxygen isotopic characteristics of zircons from proterozoic to Cretaceous in the study area, note that Precambrian zircons show a negative correlation (increase in δ18O with time).
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Figure 7. Plot of zircon εHf(t) values versus U–Pb ages for the Magmatic rocks of Zijinshan area. (a) Hf isotopic characteristics of Zircons from the Jurassic to Cretaceous period; (b) Hf zircons from proterozoic to Cretaceous. the ranges for DM, crust, and LC from reference [42].
Figure 7. Plot of zircon εHf(t) values versus U–Pb ages for the Magmatic rocks of Zijinshan area. (a) Hf isotopic characteristics of Zircons from the Jurassic to Cretaceous period; (b) Hf zircons from proterozoic to Cretaceous. the ranges for DM, crust, and LC from reference [42].
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Figure 8. Hf two-stage model age distribution histograms.
Figure 8. Hf two-stage model age distribution histograms.
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Zhang, W.; Wang, L.; Lv, X.; Li, X.; Yan, S.; Nie, J. Origin of Mesozoic Porphyritic Rocks and Regional Magmatic Evolution in the Zijinshan Ore Field of Fujian Province, China: Hf-O Isotope Characteristics of Magmatic Zircons. Minerals 2020, 10, 1143. https://doi.org/10.3390/min10121143

AMA Style

Zhang W, Wang L, Lv X, Li X, Yan S, Nie J. Origin of Mesozoic Porphyritic Rocks and Regional Magmatic Evolution in the Zijinshan Ore Field of Fujian Province, China: Hf-O Isotope Characteristics of Magmatic Zircons. Minerals. 2020; 10(12):1143. https://doi.org/10.3390/min10121143

Chicago/Turabian Style

Zhang, Wenhui, Liyuan Wang, Xupeng Lv, Xiaomin Li, Shuaiqi Yan, and Juntao Nie. 2020. "Origin of Mesozoic Porphyritic Rocks and Regional Magmatic Evolution in the Zijinshan Ore Field of Fujian Province, China: Hf-O Isotope Characteristics of Magmatic Zircons" Minerals 10, no. 12: 1143. https://doi.org/10.3390/min10121143

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