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Article

Genesis and Tectonic Implications of Early Cretaceous Granites in the Haobugao Area, Southern Great Xing’an Range: Insights from Zircon U–Pb Geochronology, Hf Isotopic Composition, and Petrochemistry

by
Mengling Li
1,2,
Henan Yu
1,2,
Yi Tian
3,
Haixin Yue
1,2,
Yanping He
1,2,
Yingbo Yu
4 and
Zhenjun Sun
1,2,*
1
School of Earth Sciences, Institute of Disaster Prevention, Langfang 065201, China
2
Hebei Key Laboratory of Earthquake Dynamics, Langfang 065201, China
3
Liaoning Geological and Mineral Survey Institute Co., Ltd., Shenyang 110032, China
4
Cores and Samples Center of Natural Resources, China Geological Survey, Langfang 065201, China
*
Author to whom correspondence should be addressed.
Minerals 2024, 14(11), 1139; https://doi.org/10.3390/min14111139
Submission received: 19 September 2024 / Revised: 7 November 2024 / Accepted: 8 November 2024 / Published: 11 November 2024
(This article belongs to the Special Issue Genesis and Metallogeny of Non-ferrous and Precious Metal Deposits, 2nd Edition)
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Abstract

:
In the Huanggangliang–Ganzhuermiao metallogenic belt in the southern Great Xing’an Range, the Haobugao Pb–Zn deposit is the most widespread skarn-type polymetallic deposit. The observed mineralization processes in this area are closely associated with both magmatic and tectonic activity. The zircon U–Pb ages of two granitoid phases are 134.0 ± 0.6 Ma and 133.4 ± 0.9 Ma (Early Cretaceous). High SiO2 content (average mass fractions of 77.98 wt.% and 73.25 wt.%), high alkalinity (average mass fractions of 6.19 wt.% and 8.78 wt.%), and low CaO levels (average mass fractions of 0.16 wt.% and 0.12 wt.%) are characteristic of these rocks. They are also enriched in high-field-strength elements (HFSEs) (Th, U, Ta, Zr, Hf, etc.) and depleted in large ion lithophile elements (LILEs) (Ba, Sr, etc.). Furthermore, the Nb/Ta ratios (7.80~8.82, 10.00~10.83) point to a crustal origin of the magma. The zircon Hf isotopic compositions suggest that the melting of young crust derived from Meso-Neoproterozoic and Neoproterozoic depleted mantle gave rise to the magma in these granite porphyries. These rocks formed in an extensional environment driven by the subduction and retreat of the Paleo-Pacific plate during the Early Cretaceous.

1. Introduction

Granites, as principal components of the continental crust and forms of igneous rocks that originate deep within the crust, are crucial for understanding the modes of formation, evolution, and growth of the continental crust [1,2,3,4,5,6,7,8,9,10]. Moreover, granites are intimately associated with the genesis of various ore deposits (e.g., tungsten, tin, uranium, molybdenum), thereby providing critical insights for the exploration and exploitation of mineral resources [11,12]. Despite extensive studies, the mechanisms of the granitic magma evolution, petrogenesis, and provenance of granites remain a major research topic [2,6,13,14,15,16].
The southern Great Xing’an Range (GXR), situated to the east of the Central Asian Orogenic Belt, is a significant nonferrous metallogenic province in northern China [17,18,19]. This region has been influenced by tectonic interactions of the Paleo-Asian, Paleo-Pacific, and Mongolia–Okhotsk tectonic systems since the Paleozoic (Figure 1).
Due to complex tectonic evolution and intense magmatic activity, many metallic mineral deposits formed (Figure 1), e.g., the Damogutu Sn–Fe deposit [22], the Dashishan Sn–Pb–Zn deposit [22], the Laojiagou Mo deposit [23], the Haobugao Pb–Zn deposit [24,25], and the Yaoertu Pb–Zn–Ag deposit [26]. At the same time, different intrusive rock types formed in the region during different mineralization periods. Therefore, this area became an ideal place for studying mineralization, magma source changes, and tectonic evolution related to mineralization. Since the 1950s, not only have the ore-forming age, ore-forming fluid characteristics, and sources of individual deposits in this area been studied by previous researchers [27,28,29,30,31], but research on the chronology, petrogenesis, and tectonic environment of metallogenic intrusive rocks has also been carried out [22,32,33,34,35,36,37,38]. These findings indicate that the Late Mesozoic was the most important period for metallogenic formation. The tectonic environment changed from interactions between a Paleo-Asian and Paleo-Pacific tectonic system to a Pacific tectonic system during this period. Many generations of intrusive rocks formed, but Early Cretaceous granite is the most widespread intrusive rock in this area [37,39,40]. However, whether the change in the tectonic environment during the Late Mesozoic was controlled by the Paleo-Pacific or Mongolian-Okhotsk tectonic system is controversial [37,38,41,42,43,44,45]. To address this issue, it is essential to first understand the regional magmatic–tectonic evolution and patterns. Consequently, this work focuses on granites in the Haobugao deposit, the largest Cu–Fe–Pb–Zn polymetallic deposit in the southern GXR, and employs petrochemistry and isotope geochemistry to further ascertain the origin and emplacement age of these granites.

2. Geological Setting

The southern GXR is located in the Xingmeng Orogenic Belt in the eastern Central Asian Orogenic Belt, which separates the Siberian plate and North China plate (Figure 1a), and is believed to be the largest block of juvenile crust formed in the Phanerozoic [46]. It is one of the most important tin-polymetallic ore districts in North China and is dominated by N–E-, N–W-, and E–W-trending structures. The strata in this area are well exposed, including the Proterozoic erathem, Silurian system, Carboniferous system, Permian system, Mesozoic erathem, and Quaternary system strata [47]. The region has undergone three significant tectonic events: the formation of the late Paleozoic Paleo-Asian tectonic domain, the stage of interaction between the Pacific Rim tectonic domain and the Paleo-Asian tectonic domain, and the stage of activity within the Mesozoic–Cenozoic Pacific Rim tectonic domain. These events led to the development of large-scale fault and fold structures in the area [48,49,50], which has been influenced by Yanshanian tectonic movement since the Mesozoic. Magmatic activity throughout the southern section was intense, with granitic intrusive rocks being particularly prevalent (Figure 1b). These granites can be divided into Hercynian, Indosinian, and Yanshanian granites based on their formation periods. The Yanshanian granites are the most widespread and are important for understanding the genesis and sources of regional mineralization.
The Haobugao Pb–Zn deposit is the largest polymetallic deposit in the Huanggangliang–Ganzhuermiao polymetallic mineralization belt, and 143~135 Ma is the most important mineralization period [36]. The exposed strata of the Haobugao deposit mainly comprise the Middle Permian Dashizhai and Zhesi Formations, the Upper Jurassic Manketou’ebo Formation, and Quaternary loose sediments [47] (Figure 1c). The Dashizhai Formation is the main ore-bearing stratum, and the Manketou’ebo Formation unconformably covers it at various angles [40]. Due to the influence of Late Paleozoic orogeny and Mesozoic tectonic activities, the area has highly developed structures such as folds and faults (Figure 1b), which provide favorable conditions for mineralization.

3. Materials and Methods

3.1. Field and Petrographical Investigation

The samples were collected in the northern Haobugao deposit, and their lithologies are granite porphyries B02 (119°30′15″ E, 44°34′50″ N) and B10 (119°31′15″ E, 44°33′30″ N) (Figure 1c and Figure 2). The B02 granite porphyry vein intrudes into the upper and lower strata. The lower stratum is the Permian Dashizhai Formation and consists of intermediate-to-acidic lava, slate, silty slate, and sand conglomerate, and the upper stratum is acidic tuff of the Jurassic Manketou’ebo Formation. The granite porphyry vein is about 8 m wide. The B10 granite porphyry vein is about 2 m wide and also shows an intrusive relationship with the strata. The stratum is the Permian Zhesi Formation and consists of sandy conglomerate, silty slate, and slate. In this study, a total of 10 samples were collected from these two veins, including 5 samples of B02 and 5 samples of B10. Six thin sections were examined from these rocks, and classification was achieved through hand-collected specimens investigated using a Leica transmitted–reflected polarizing microscope. In addition, major element and trace element analyses were conducted on all 10 samples, and zircon was separated from all samples for zircon U–Pb age dating and in situ Hf isotopic composition analysis.

3.2. Analytical Methods

The zircon grain extraction, cathodoluminescence imaging, U–Pb dating, Hf isotopic composition analyses, and whole-rock major and trace element analyses of intrusive rock were completed at Yanduzhongshi Geological Analysis Laboratories, Ltd., Beijing, China.
Zircon U–Pb isotopes were analyzed by laser ablation–inductively coupled plasma–mass spectrometry (LA–ICP–MS). The laser ablation microprobe used was a NWR193 (Elemental Scientific Lasers, Bozeman, MT, USA), and the inductively coupled plasma–mass spectrometer (ICP–MS) was an M90 (Analytikjena, Jena, Germany). To adjust the sensitivity, helium was used as the carrier gas and argon gas was used as the compensation gas during the laser ablation process. Both gasses were mixed in a Y-shaped junction before entering the ICP instrument. Every time-resolved analysis included an approximately 20~30 s blank signal and a 40 s sample signal. The trace element contents of the zircon were quantified using SRM610 as an external standard and Si as an internal standard [51]. The zircon U–Pb ages were quantified using Plesovice [52] as an external standard, and 91500 zircon [53] was analyzed between every 8 unknown samples for quality control. Off-line processing of data was completed using the software ZSkits 2.0 [54], including selection of samples and blank signals, drift correction of instrument sensitivity, and calculation of elemental contents and U–Th–Pb isotope ratios and ages. The calculation of weighted average ages and plotting of concordia diagrams were completed with Isoplot 4.15 [55]. Age uncertainties are quoted at the 95% (1σ) confidence level. According to the real-world situation, the testing denuded diameter was selected as 25 μm. The analytical results are shown in Table S1.
Before whole-rock major and trace element analyses, the samples were broken into centimeter sizes, washed with deionized water, dried, and then ground to less than a 200 mesh (0.5200 ± 0.0001 g). The major elements were analyzed using X-ray fluorescence (XRF) spectroscopy, with an analytical accuracy of better than 1%. The trace elements were analyzed using ICP–MS (M90, Analytikjena, Jena, Germany), with an accuracy of better than 10%. The analytical results are shown in Table S2.
The Hf isotopic compositions of the zircon samples were analyzed using a multicollector inductively coupled plasma–mass spectrometry (MC–ICP–MS) instrument (Neptune-plus, Thermo Electron Corporation, Waltham, MA, USA) and a laser ablation sampling system (NWR193, Elemental Scientific Lasers, Bozeman, MT, USA). A stationary spot was used for the present analyses, with a beam diameter of 35 μm. For the test procedure and calibration method, refer to Wu et al. [56]. Plesovice and 91500 zircon standards were used during the analyses. tDM1 and tDM2 were calculated for each sample as described by references [57,58]. The analytical results are shown in Table S3.

4. Results

4.1. Petrography

The weathered surface of the granite porphyry B02 is a khaki color, and it has a porphyritic texture and vein structure; the veins are quartz veins (Figure 3a,b). The main minerals are plagioclase (60~65 vol%) and quartz (20~25 vol%), with minor levels of pyrite (2~5 vol%). Some plagioclase has undergone sericitic alteration, and many dark edges of the feldspars turned yellow-brown after being dyed (Figure 3a,b). The weathered surface of the granite porphyry B10 is a khaki color, and it has a porphyritic texture and massive structure (Figure 3c,d). The main minerals are plagioclase (45~50 vol%) and quartz (15~20 vol%), and the matrix is plagioclase. In the photomicrographs, plagioclase has typical polysynthetic twinning and has undergone partial sericitic alteration. The matrix also has a certain radial arrangement (Figure 3c).

4.2. Zircon U–Pb Dating

The zircon U–Pb isotopic compositions of B02 and B10 are shown in Table S1. The cathodoluminescence (CL) images (Figure 4) reveal that the zircon samples have a zonal structure and magmatic zircon characteristics [59]. The zircon samples’ lengths range from 50 μm to 150 μm, and the length-to-width ratios range from 3:2 to 3:1. High U levels will lead to increased radiation damage, which quenches the CL response. The CL images of the B02 zircon are darker than those of the B10 zircon, which indicates that the zircon U and Th contents in the B02 samples are higher than those in the B10 samples [60]. The Th/U ratio of zircon grains has been used as a method to help distinguish their growth process (e.g., metamorphic versus magmatic zircon). The Th/U ratios of the zircon of the granite porphyries B02 and B10 are 0.40~0.78 and 0.28~0.77 (averages of 0.59 and 0.46), respectively, indicating a probable magmatic origin [61,62].
The zircon U–Pb system has a high temperature and weathering resistance, which are beneficial for preserving the isotopic composition of magma at the beginning of crystallization [63,64]. Therefore, the zircon crystallization age represents the rock formation age. The 238U/206Pb weighted mean age of the zircon from the granite porphyry B02 is 134.0 ± 0.6 Ma (n = 23, mean standard weighted deviation (MSWD) = 0.92), and that of the zircon from granite porphyry B10 is 133.4 ± 0.9 Ma (n = 12, MSWD = 0.54) (Figure 5), so these formed in the Early Cretaceous. This information can be used to study the source areas of metal mineral enrichment during the same period.

4.3. Major and Trace Element Compositions

The major element compositions of granite porphyries B02 and B10 are shown in Table S2. All samples are plotted in the subalkaline granite region in the (K2O + Na2O) vs. SiO2 classification (Figure 6a). The B10 samples were plotted in the transition region between the shoshonite series and the high-potassium calc-alkaline series, whereas most of the B02 samples were plotted in the high-potassium calc-alkaline series in the K2O vs. SiO2 classification (Figure 6b). The rock composition is close to that of calc-alkaline rhyolite, which is consistent with the petrographic identification results. All samples are strongly peraluminous (Figure 6c). On the Harker diagrams (Figure 7), Al2O3, total Fe2O3 and TiO2 show a negative correlation with SiO2, while MgO shows a positive correlation with SiO2, and CaO, Na2O and K2O show large variations without a clear trend.
The trace element compositions of the granite porphyries B02 and B10 are shown in Table S2. Primitive mantle-normalized trace element spider diagrams (Figure 8a) show that these rocks are obviously depleted in Ba, Nb, Sr, P and Ti and enriched in Rb, Th, U, Ta, Nd, Zr, and Hf. Compared to B10, B02 has lower concentrations of Zr, Hf and rare earth elements (REEs). These samples have obvious right-dipping types, high differentiation of LILEs and HREEs (LREEs/HREEs = 10.77~13.67 and 4.82~6.64, respectively) and strong negative Eu anomalies (δEu values of 0.38~0.48 and 0.29~0.37) (Figure 8b). The (La/Sm)N ratios are 3.19~5.91 and 2.56~3.37, and the (La/Yb)N ratios are 2.85~21.17 and 3.16~6.35, respectively.

4.4. Zircon Hf Isotopes

The compositions of the zircon Hf isotopes are shown in Table S3 and plotted in Figure 9. The zircon from B02 showed the initial 176Hf/177Hf ratios of 0.282824~0.282902, and the εHf(t) values ranged from +4.59 to +7.34. The two-stage model ages (tDM2) were in the range of 718~895 Ma. The zircon from B10 showed initial 176Hf/177Hf values of 0.282717~0.282861, and the εHf(t) values ranged from +0.86 to +5.99. The two-stage model ages (tDM2) were in the range of 807~1134 Ma.

5. Discussions

5.1. Diagenetic and Metallogenic Epochs and Magmatic Evolution

Previous studies have shown that the metallogenic epoch of the Haobugao deposit and its surrounding deposits was concentrated during 143~135 Ma [71,72,73], and some deposits formed after 133 Ma [74]. Magmatic activity is very strong in the southern GXR, and acidic magmatic rocks are the main rocks in this region (Figure 1b). Therefore, many researchers have reported different granites in the Haobugao deposit and its surrounding areas, including Daitongshan fine-grained granite (265 ± 5 Ma) [75], Meng’entaolegai biotite granite (250 ± 1 Ma) [34], Baiyinnuoer granodiorite porphyry (171 Ma) [76], Shijiangshan monzogranite (160 ± 1, 143 ± 1 and 136 ± 1 Ma) [77], Shuangjianzishan granite (159 ± 2 Ma) [78], Bengbuleng granodiorite (150 ± 1 Ma) and granite (145 ± 1 Ma) [73], Xiaohanshan monzogranite (144 ± 1 Ma) [79], Wulanchulute granite (142 ± 1 and 140 ± 1 Ma) [40], Wulandaba monzogranite (137 ± 1 Ma) [80], Haobugao mineralized granite (140 ± 1 Ma), post-mineralized granite (131 ± 1 Ma) [81], Huanggang granite porphyry (137 ± 1 Ma) [82] and Menghewula granite (134 ± 1 Ma) [73]. A large amount of evidence indicates that the most intense period of magmatic activity in this area occurred 145~125 million years ago (Figure 10, Table S4). In a recent study, Hu [73] divided the metallogenic granites of the Haobugao Pb–Zn deposit into three magmatic evolutionary periods, namely, 150~145 Ma, 143~135 Ma and approximately 130 Ma, according to the relationships, genesis, formation age, metallogenic age and tectonic setting between various rocks and ore bodies. However, the LA–ICP–MS zircon U–Pb dating results for Haobugao granite porphyries B02 and B10 reveal that the weighted average 206Pb/238U ages are 134.0 ± 0.6 Ma and 133.4 ± 0.9 Ma (Early Cretaceous, Figure 5). Compared with previous studies, this study divides the magmatic evolutionary period into three stages: 152~150 Ma, 146~138 Ma and 134~131 Ma. The granite porphyries B02 and B10 formed in the third stage, which was later than the Haobugao metallogenic granite, and formed in the same intrusive period.

5.2. Origin and Development of Volcanic Rocks

As the most popular one among approximately twenty different granite classification schemes evolved over the past several decades, granites are classified according to the properties of their magma source area [1,2,3,4,5,6]; they are divided into I (intracrustal or igneous)-, S (supracrustal or sedimentary)-, M (mantle-derived)-, and A (alkaline, anorogenic, and anhydrous)-type granites, and different types of granites exhibit different geochemical characteristics. M-type granites have relatively high Cr, Ni and Co levels; I-type granites have low SiO2, Al2O3, A/CNK and Fe2O3t levels; and S-type granites have high Al2O3, K2O and P2O5 levels and Al saturation index values >1.1. However, A-type granites are considered to have formed in high-temperature, low-oxygen-fugacity, anhydrous and non-orogenic/post-orogenic environments, and they have obvious negative Eu anomalies [83,84] and high Fe/(Fe + Mg), A/NK, K2O/Na2O and Ga/Al ratios. Many researchers have studied granites in and around Haobugao, showing that this area contains granites with a wide range of epochs, and the most important metallogenic epoch was Jurassic–Cretaceous in the Haobugao area [73]. These granites that formed in the Late Paleozoic–Mesozoic are mainly A-type granites [82], whereas the Late Mesozoic granites are mainly highly differentiated I-type granites [80].
The elemental characteristics of granite porphyries B02 and B10 show high SiO2, K2O, Fe/(Fe + Mg), A/NK, K2O/Na2O and Ga/Al ratios and are Na-rich, Ca-poor, enriched in Rb, Th, U, Ta, Nd, Zr and Hf and depleted in Ba, Sr, P, Eu and Ti. These characteristics are similar in A-type granites [38,40,77]. Y and Nb are depleted compared to other A-granites because of the amphiboles and other minerals crystallized during the formation of the Haobugao granite porphyry [85]. P and Ti are depleted because of the separation and crystallization of minerals (such as apatite, titanite, etc.). Ba and Sr are also depleted, which indicates the separation of plagioclase, biotite and other minerals in the process of partial melting or crystallization differentiation. But B02 and B10 are different in some ways. B02 had a lower Fe/Mg ratio than B10. So, B02 was crystallized at a higher oxygen fugacity [86]. B02 had a lower Zr content because more zircons separated and crystallized. In the Zr vs. 10,000Ga/Al diagram, B10 is plotted in the area with A-type granites, and B02 is plotted in the area with overlapping I- and S-type-differentiated granites and A-type granites (Figure 11a). In the Ce vs. Nb vs. Y diagram (Figure 11b), they are both plotted in the apotectonic A-type (A2) granite area; the Y/Nb ratios of B02 and B10 are 1.4~2.86 and 2.37~2.64, and they are post-orogenic granites (with Y/Nb > 1.2) [84,87]. Due to the highly differentiated (I/S-type) granites and the fact that aluminum A-type granites are difficult to distinguish, further discrimination is required for these granites. Firstly, the Zr/Hf ratios of B02 and B10 are 27.75~31.16 and 34.49~38.37, classifying them as mid-differentiated granites [88], and the degree of differentiation of B10 is slightly less than that of B02. Moreover, highly differentiated granites often have extremely low Zr content [89], and I-type granites have extremely low P2O5 contents (<0.01 wt.%), which are negatively correlated with SiO2 [90]. There is no significant correlation between P2O5 and SiO2 in these samples (Figure 7h), and there is a positive correlation between Zr and 10,000Ga/Al. In addition, the zircon saturation thermometry (TZr) of I-type granites is generally lower than 800 °C [91]. According to Watson and Harrison [92], the TZr of B10 is 862~873 °C, and that of B02 is 793~814 °C, among which only one sample has a value lower than 800 °C. A-type granites are generally considered to originate from relatively high-temperature magma [93]. To sum up, the Haobugao granites are considered A-type granites.
The petrogenesis of A-type granites has been debated because they have similar mineralogical and compositional characteristics but occur in vastly different tectonic environments (from continental margin to oceanic island) [1,6,84,85,87,93,94]. There are four main views on the formation mechanism of A-type granites: (1) crystallization differentiation of mantle-derived alkaline basaltic magma [87]; (2) crust-mantle magmatic mixing [7,94]; (3) partial melting of the middle–upper crust in silicoaluminate [95,96,97]; and (4) partial melting of the lower crust caused by mantle-derived intrusive magma [2,6]. A-type granites formed via magma crystallization differentiation of mantle-derived alkaline basalts. They are often related to intermediate and basic magma and exhibit hyperalkaline characteristics. However, the granite porphyries in the Haobugao area are peraluminous, high in SiO2, and have low MgO, Ni and Co contents, which indicate that mantle-derived materials had little influence on their formation. The Rb/Sr ratios (2.57~4.74, 3.24~5.11), Nb/La ratios (0.13~1.43, 0.38~0.70) and Nb/Ta ratios (7.80~8.82, 10.00~10.83) of granite porphyries B02 and B10 are crustal [68,98,99]. Therefore, the magma sources of the Early Cretaceous granite porphyries are predominantly believed to be crustal.
In recent years, cassiterite has been found locally in the Haobugao skarn, which has attracted much attention in terms of Sn mineralization. Sn is moderately incompatible during partial melting of the mantle and is depleted in the mantle and enriched in the crust, whereas its geochemical properties are controlled by source composition, oxygen fugacity, volatile matter content and magmatic crystallization differentiation during magmatism [12,100,101,102,103,104,105]. Sn is enriched in magma with a high degree of crystallization differentiation; that is, Sn mineralization is related mainly to acidic magmatic activity. More than 99% of Sn deposits in the world are directly or indirectly related to granite [25,106,107], so Sn mineralization is considered closely related to A-type granites [38,108,109,110,111,112,113]. Research shows that there is a close relationship between Pb–Zn polymetallic mineralization in the Haobugao area and the regional A-type granites.
In situ Hf isotopic analysis of zircon can be used to reveal crustal evolution and trace magma source areas [114]. The 176Yb/177Hf ratios of zircon from granite porphyries B02 and B10 are far lower than 1.2 and are characteristic of crust–mantle mixing. However, most of the 176Lu/177Hf ratios are less than 0.002, which indicates that zircon has a low accumulation of radioactive Hf after formation. εHf(t) > 0 indicates that the magma originated from depleted mantle or young crust derived from depleted mantle [115]. Previous studies have shown that zircons from Early Cretaceous granites in the southern GXR have positive εHf(t) values and young two-stage crustal model ages (tDM2). The results show that the magma source areas of these granites all originated from the partial melting of newly formed continental crust in the Paleozoic–Neoproterozoic, and this crust contained many mantle-derived materials [37,73,82]. The two-stage model ages (tDM2) of B02 and B10 are 718~895 Ma and 807~1134 Ma, respectively, which suggests that more ancient crustal materials may have contributed to the B10 porphyry. In the diagram of εHf(t) vs. age (Figure 9), all εHf(t) values of the zircon are plotted between the evolutionary lines of depleted mantle and crust. Therefore, the magma source area of the granite porphyries B02 and B10 includes newly formed crust from Neoproterozoic and Meso-Neoproterozoic depleted mantles, respectively.

5.3. Tectonic Implications

Because the Haobugao Pb–Zn deposit is the largest polymetallic deposit in the Huanggangliang–Ganzhuermiao polymetallic metallogenic belt, the geodynamic study of granite porphyries B02 and B10 has economic significance. The granite porphyries B02 and B10 are enriched in HFSEs (Th, U, Ta, Zr, Hf, etc.) and depleted in LILEs (Ba, Sr, etc.), similar to rocks produced in continental rift extensional environments and stable continental plates. The Y–Nb–Ce diagram (Figure 11b) suggests that they formed in a post-orogenic environment. In Figure 12, all samples are plotted in the post-COLG region and are post-orogenic granites. According to previous studies, the Mongolia–Okhotsk and Paleo-Pacific tectonic systems developed simultaneously in the GXR from the Middle to Late Jurassic. During the Late Jurassic to Early Cretaceous, a collision occurred in the eastern Mongolia–Okhotsk suture zone [116]. Magmatism and mineralization in this area mostly spread along the suture zone [81]. The above illustrates that the southern GXR area changed from a collisional orogenic environment to a post-orogenic extensional environment in the Late Mesozoic [117,118]. Moreover, research on volcanic rocks has revealed that this region was in a post-orogenic extensional environment in the Early Cretaceous [37,38], so the granite porphyries in the Haobugao area formed in an extensional environment after the collisional orogeny. There are three main dynamic models for modeling magmatic activity in North China since the Jurassic [41,119], among which the Paleo-Pacific plate subduction model matches the characteristics of magmatic activity. Owing to the subduction and retreat of the Paleo-Pacific plate, the tectonic system of the southern GXR changed with the processes of decompression and warming. The heat provided by the upwelling of mantle materials caused the overlying newly developed crust to partially melt and finally formed these rocks.
In combination with previous studies, the tectonic evolution of the Haobugao area can be divided into three stages: the oceanic–continental subduction stage (Carboniferous–Late Permian), the collisional orogenic stage (Early Triassic–early stage of Early Cretaceous) and the post-collisional stage (late stage of Early Cretaceous). The oceanic–continental subduction stage was a bidirectional subduction period from the Paleo-Asian Ocean to the North China Craton and Siberian Craton, during which many magmatic rocks, including the Bairendaba granodiorite and Wulantaolegai K-feldspar granite, formed [34]. During the collisional orogenic stage, the Paleo-Asian Ocean closed, the North China Craton collided with the Siberian Craton, and the Haobugao area changed from a subduction environment to a collisional orogenic environment. During this period, magmatic rocks, such as Daitongshan granite, Meng’entaolegai biotite granite, Zhuanshanzi monzogranite and Laojiagou monzogranite porphyry, formed [23,34,49,75]. During the post-collisional stage, the tectonic environment changed to an extensional environment. During this period, the Xiaohanshan monzogranite, Wulandaba granodiorite, Huaganzigou monzogranite and Hansumu monzogranite formed [73,79,121,122], and the Haobugao Pb–Zn deposit, Huanggangliang Sn–Fe deposit, Budunhua Cu deposit and other deposits developed [71,72]. Many granites formed during different stages of magmatic evolution during this period.

6. Conclusions

(1) The LA–ICP–MS zircon U–Pb ages of the granite porphyries B02 and B10 in the Haobugao area are 134.0 ± 0.6 Ma and 133.4 ± 0.9 Ma, respectively, both of which formed in the Early Cretaceous and were intrusive during the same period.
(2) These two types of granite have similar geochemical characteristics, such as being Si-rich, K-rich, Na-rich and Ca-poor, and are high-K calc-alkaline rocks. Moreover, they are enriched in HFSEs (Th, U, Ta, Zr, Hf, etc.), depleted in LILEs (Ba, Sr, etc.) and have the characteristics of apotectonic A-type granites.
(3) The magma source of the B02 porphyry was the partial melting of newly formed crust in the Neoproterozoic, whereas that of the B10 porphyry was the partial melting of newly formed crust in the Meso-Neoproterozoic. They are the products of the partial melting of newly generated crust caused by mantle-derived heat.
(4) This area was in the post-collisional stage in the Early Cretaceous, and the granite porphyries B02 and B10 formed in an extensional environment driven by the subduction and retreat of the Paleo-Pacific plate.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/min14111139/s1, Table S1: LA-ICP-MS U-Pb dating results of zircon in granite porphyries B02 and B10 from Haobugao; Table S2: Major and trace element compositions of granite porphyries B02 and B10; Table S3: Zircon Hf isotopic compositions of granite porphyries B02 and B10; Table S4: Diagenetic age of granites in the southern GXR [123,124,125,126].

Author Contributions

Conceptualization, M.L. and Z.S.; methodology, H.Y. (Henan Yu); software, M.L. and H.Y. (Henan Yu); investigation, Y.T., H.Y. (Haixin Yue), Y.Y. and Z.S.; resources, Z.S.; data curation, M.L. and Y.H.; writing—original draft preparation, M.L.; writing—review and editing, Z.S. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the Fundamental Research Funds for Central Universities of China (Grant Number ZY20215129) and the Langfang Science and Technology Research and Development Plan Self-funded Project (Grant Number 2023013091).

Data Availability Statement

Data are contained within the article and Supplementary Materials.

Acknowledgments

We sincerely appreciate the detailed and constructive reviews and suggestions from anonymous reviewers.

Conflicts of Interest

Author Yi Tian was employed by the company Liaoning Geological and Mineral Survey Institute Co., Ltd. The remaining authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

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Figure 1. Location map of the southern Great Xing’an Range (a), modified from [20]); geological map of distribution of magmatic rocks (b), modified from [21]), and (c) location map of sample locations in this study.
Figure 1. Location map of the southern Great Xing’an Range (a), modified from [20]); geological map of distribution of magmatic rocks (b), modified from [21]), and (c) location map of sample locations in this study.
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Figure 2. Photos of granite porphyries B02 and B10. The (a,b) are natural outcrops of granite porphyries.
Figure 2. Photos of granite porphyries B02 and B10. The (a,b) are natural outcrops of granite porphyries.
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Figure 3. Photomicrographs of selected samples from granite porphyries B02 (a,b) and B10 (c,d). Pl: plagioclase; Qtz: quartz; Py: pyrite.
Figure 3. Photomicrographs of selected samples from granite porphyries B02 (a,b) and B10 (c,d). Pl: plagioclase; Qtz: quartz; Py: pyrite.
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Figure 4. Representative cathodoluminescence (CL) images and 206Pb/238U ages of zircon from granite porphyries B02 and B10.
Figure 4. Representative cathodoluminescence (CL) images and 206Pb/238U ages of zircon from granite porphyries B02 and B10.
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Figure 5. U–Pb concordia diagrams and weighted mean graph for zircon from granite porphyries. (a,b) granite porphyry B02; (c,d) granite porphyry B10. The units for the mean numbers are Ma.
Figure 5. U–Pb concordia diagrams and weighted mean graph for zircon from granite porphyries. (a,b) granite porphyry B02; (c,d) granite porphyry B10. The units for the mean numbers are Ma.
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Figure 6. Petrogenetic classification diagrams for the Early Cretaceous granite porphyries B02 and B10 and their major element characteristics. (a) Total alkali vs. SiO2 classification (TAS, from [65]); (b) K2O vs. SiO2 classification, from [66]; (c) A/NK vs. A/CNK classification, from [67]. A/NK = Al2O3/(Na2O + K2O), A/CNK = Al2O3/(CaO + Na2O + K2O).
Figure 6. Petrogenetic classification diagrams for the Early Cretaceous granite porphyries B02 and B10 and their major element characteristics. (a) Total alkali vs. SiO2 classification (TAS, from [65]); (b) K2O vs. SiO2 classification, from [66]; (c) A/NK vs. A/CNK classification, from [67]. A/NK = Al2O3/(Na2O + K2O), A/CNK = Al2O3/(CaO + Na2O + K2O).
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Figure 7. Major and trace element Harker variation diagrams showing the magmatic evolution of granite porphyries B02 and B10. Pl: plagioclase, Hbl: hornblende, Bt: biotite, Kfs: K-feldspar. (a–h) variation trend of TiO2, Al2O3, Fe2O3t, MgO, CaO, Na2O, K2O and P2O5 with SiO2 in granite porphyries; (i,j) variation trend of Ba and Rb with Sr in granite porphyries.
Figure 7. Major and trace element Harker variation diagrams showing the magmatic evolution of granite porphyries B02 and B10. Pl: plagioclase, Hbl: hornblende, Bt: biotite, Kfs: K-feldspar. (a–h) variation trend of TiO2, Al2O3, Fe2O3t, MgO, CaO, Na2O, K2O and P2O5 with SiO2 in granite porphyries; (i,j) variation trend of Ba and Rb with Sr in granite porphyries.
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Figure 8. Primitive mantle-normalized trace element diagrams (a) and chondrite-normalized REE patterns (b) of granite porphyries B02 and B10. The values for primitive mantle and chondrite were obtained from Sun and McDonough [68] and Taylor and McLennan [69], respectively.
Figure 8. Primitive mantle-normalized trace element diagrams (a) and chondrite-normalized REE patterns (b) of granite porphyries B02 and B10. The values for primitive mantle and chondrite were obtained from Sun and McDonough [68] and Taylor and McLennan [69], respectively.
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Figure 9. Correlations between εHf(t) and ages of zircon from granite porphyries B02 and B10. The diagrams are based on the study in [70].
Figure 9. Correlations between εHf(t) and ages of zircon from granite porphyries B02 and B10. The diagrams are based on the study in [70].
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Figure 10. Relative probability plot for granites in the southern GXR.
Figure 10. Relative probability plot for granites in the southern GXR.
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Figure 11. Zr vs. 10,000Ga/Al (a) and Ce vs. Nb vs. Y (b) plots for granite porphyries B02 and B10. A1: anorogenic A-type granites; A2: apotectonic A-type granites. The diagrams are based on the studies [10,84,87].
Figure 11. Zr vs. 10,000Ga/Al (a) and Ce vs. Nb vs. Y (b) plots for granite porphyries B02 and B10. A1: anorogenic A-type granites; A2: apotectonic A-type granites. The diagrams are based on the studies [10,84,87].
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Figure 12. The tectonic discrimination diagrams of granite porphyries B02 and B10. VAG: volcanic arc granites; ORG: oceanic ridge granites; WPG: within-plate granites; syn-COLG: syn-collisional granites; post-COLG: post-collisional granites. The diagrams are based on the studies [67,120].
Figure 12. The tectonic discrimination diagrams of granite porphyries B02 and B10. VAG: volcanic arc granites; ORG: oceanic ridge granites; WPG: within-plate granites; syn-COLG: syn-collisional granites; post-COLG: post-collisional granites. The diagrams are based on the studies [67,120].
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Li, M.; Yu, H.; Tian, Y.; Yue, H.; He, Y.; Yu, Y.; Sun, Z. Genesis and Tectonic Implications of Early Cretaceous Granites in the Haobugao Area, Southern Great Xing’an Range: Insights from Zircon U–Pb Geochronology, Hf Isotopic Composition, and Petrochemistry. Minerals 2024, 14, 1139. https://doi.org/10.3390/min14111139

AMA Style

Li M, Yu H, Tian Y, Yue H, He Y, Yu Y, Sun Z. Genesis and Tectonic Implications of Early Cretaceous Granites in the Haobugao Area, Southern Great Xing’an Range: Insights from Zircon U–Pb Geochronology, Hf Isotopic Composition, and Petrochemistry. Minerals. 2024; 14(11):1139. https://doi.org/10.3390/min14111139

Chicago/Turabian Style

Li, Mengling, Henan Yu, Yi Tian, Haixin Yue, Yanping He, Yingbo Yu, and Zhenjun Sun. 2024. "Genesis and Tectonic Implications of Early Cretaceous Granites in the Haobugao Area, Southern Great Xing’an Range: Insights from Zircon U–Pb Geochronology, Hf Isotopic Composition, and Petrochemistry" Minerals 14, no. 11: 1139. https://doi.org/10.3390/min14111139

APA Style

Li, M., Yu, H., Tian, Y., Yue, H., He, Y., Yu, Y., & Sun, Z. (2024). Genesis and Tectonic Implications of Early Cretaceous Granites in the Haobugao Area, Southern Great Xing’an Range: Insights from Zircon U–Pb Geochronology, Hf Isotopic Composition, and Petrochemistry. Minerals, 14(11), 1139. https://doi.org/10.3390/min14111139

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