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Article

Zircon U–Pb Geochronology, Geochemistry and Geological Significance of the Anisian Alkaline Basalts in Gejiu District, Yunnan Province

by
Zhi Shang
and
Yongqing Chen
*
School of Earth Sciences and Resources, China University of Geosciences, Beijing 100083, China
*
Author to whom correspondence should be addressed.
Minerals 2020, 10(11), 1030; https://doi.org/10.3390/min10111030
Submission received: 6 September 2020 / Revised: 22 October 2020 / Accepted: 16 November 2020 / Published: 18 November 2020
(This article belongs to the Special Issue Detrital Mineral U/Pb Age Dating and Geochemistry of Magmatic Products in Basin Sequences: State of the Art and Progress)
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Abstract

:
The Gejiu Anisian alkaline basalts (GAAB), distributed in the southern part of the Emeishan large igneous province (ELIP), are crucial to understand the tectonomagmatic activity during the Triassic. Geochronological, geochemical, and Sr-Nd-Pb isotopic analyses were systematically applied to explore the origin, petrogenesis, and tectonic setting of the GAAB, and how they relate to the ELIP. Zircon U-Pb dating set the eruption date at 244 Ma. Most of the samples belonged to alkaline basalts and had high TiO2 (2.14–3.23 wt.%) and MgO (4.43–19.58 wt.%) contents. Large ion lithophile elements (LILEs) were enriched relative to high field strength elements (HFSEs). The rare earth elements (REEs) and trace element signatures in the normalized diagrams were similar to oceanic island basalts (OIB) and Emeishan high-Ti basalts. These samples had consistent Sr-Nd isotope compositions: the initial 87Sr/86Sr values ranged from 0.7044 to 0.7048 and εNd(t) = 3.25–4.92. The Pb isotopes were more complex, the (206Pb/204Pb)t, (207Pb/204Pb)t, (208Pb/204Pb)t ratios were 17.493–18.197, 15.530–15.722, and 37.713–38.853, respectively. Our results indicate that the GAAB originated from the deeper enriched mantle with 5% to 15% partial melting of garnet lherzolite and a segregation depth of 2 to 4 GPa (60–120 km). During the formation of the GAAB, clinopyroxene and Ti-Fe oxides were fractionally crystallized with insignificant crustal contamination. The GAAB were formed in a extensional regime that was related to the Gejiu-Napo rift event in the Triassic.

1. Introduction

Basaltic magmatism is a fundamental geological process, and of the various kinds of basalts, alkaline basalts are thought to have unique geological implications [1,2]. Massive stretches of basaltic magma are distributed along the western margin of the South China Block in SW China, making up the widely known Emeishan large igneous province (ELIP), which covers an area of over 5 × 105 km2 in SW China and northern Vietnam (Figure 1a) [3]. The basalts in the ELIP were mainly formed during the Late-Middle Permian (ca. 260 Ma) and have been identified as related to a mantle plume [4,5,6,7,8,9,10,11,12]. The Gejiu Anisian alkaline basalts (GAAB), formed later than the ELIP, are important in understanding the tectonic evolution of the western South China Block during post-ELIP tectonomagmatism.
However, the origin and mechanism behind the formation of the GAAB in the southern ELIP remain controversial and poorly understood, and the links between the GAAB and the ELIP have not been well established. Several formation mechanisms have been proposed for the GAAB, these have included an orogenic environment [13], a within-plate extensional environment [14,15], a back-arc rift basin [16,17,18,19], and a decompressive melting of the pre-existing Emeishan plume head induced by a rift event [20,21]. Nevertheless, no study has been able to provide sufficient evidence to confirm the origin or formation mechanism of the GAAB, likely due to unsystematic sampling and research methods.
In this paper, samples were collected from both outcrop and boreholes in Qilinshan and Laochang. Integrated geochronological, geochemical, and isotopic data were obtained to investigate the origin and formation mechanism of the GAAB, along with any links between the Middle Triassic igneous activity in Gejiu and the ELIP. This analytical data from the Gejiu area will contribute to a better understanding of these, as of yet, unsolved issues.

2. Geologic Background and Petrography

The Gejiu ore district is located in the South China block, East of the Ailaoshan belt [22] (Figure 1a). The collision of Indochina and South China Block took place during the Early Triassic, forming the widely known Ailaoshan suture zone, accompanied by complex tectonomagmatism [23]. It extends northwest to the Jinshajiang suture zone and southeastern to the Song Ma suture zone (Figure 1a) [24,25,26]. The Ailaoshan belt is an NW-SE striking fan-shaped area that narrows to the NW and widens to SE (500 km long, and 10 to 50 km wide) and this belt can be subdivided into Western, Central, and Eastern Ailaoshan zones from west to east [23].
The GAAB are situated in the eastern part of the Ailaoshan suture zone (Figure 1a) [3,20,21]. There are numerous faults in the Gejiu ore district (Figure 1b,c). The Gejiu fault as the southern extension of Xiaojiang fault, which has an SN-trending orientation, is the main fault dividing the Gejiu area into two sectors [22]. The secondary faults, which generally trend EW, show the signature of an equidistant distribution in the eastern sector and divide the Gejiu ore district into five main ore segments, namely the Malage, Songshujiao, Gaosong, Laochang, and Kafang from north to south (Figure 1c). The basalts of interest are primarily located in the eastern sector of the Gejiu ore district.
The Triassic GAAB cover an area of nearly 125 km2 in the south of the ELIP, and are widely distributed in the Qilinshan, Laochang, and Kafang ore segments (Figure 1c) [18,20]. The basalts in Laochang and Kafang, which are considered as a unit, are concealed under the ground, while the Qilinshan basalts are exposed at the earth’s surface. The Middle Triassic Gejiu Formation carbonates and the Falang Formation fine-grained clastic sediments and carbonates are the dominant strata (over 3000 m) in the Gejiu ore district. These basaltic lavas are found in the lower part of the Gejiu Formation where they were conformably interbedded within the Gejiu Formation. The Laochang and Kafang basalts exhibit a subhorizontal distribution with an overall dip to the northwest. The thickness of a single layer of the basalt ranges from 0.05 to 30 m, and the total thickness is about 100 m [13,21]. Due to the intrusion of the Mesozoic granitic magmatism, the basalts in Laochang and Kafang have undergone different degrees of metamorphism, forming olivine basalts with weak metamorphism and phlogopite metabasalts that have high degrees of metamorphism [17]. The Qilinshan basalts found in the eastern part of the Songshujiao ore segment underwent relatively low degrees of metamorphism and were less altered than the basalts in Laochang and Kafang.
In this research, outcrop samples were collected from Qilinshan and the borehole samples came from 1360 levels in the Laochang ore segment. Altogether, 59 samples were collected for zircon U-Pb dating, geochemical and Sr-Nd-Pb isotope analyses. The sample locations can be seen in Figure 1c,d. These basalts were dark green and had an abundance of amygdaloidal structures (Figure 2a). The oval-shaped amygdales were 0.2 to 2 cm in diameter and showed directional arrangements. These amygdales exhibited a nonuniform distribution in the basalt samples. Most of the amygdales were filled with silicic material and/or carbonate. Chloritization and actinolitization were common in the basalts. These basalts were mainly composed of pyroxene, plagioclase, olivine (Figure 2b,c), and accessory minerals such as ilmenite and magnetite. The alteration in Laochang basalts was more pervasive and severe than that in Qilinshan basalts, and the alteration minerals were mainly phlogopite, actinolite, chlorite, and tremolite (Figure 2d–f).

3. Methods

3.1. Zircon LA–ICP–MS Analyses

Thirty kilos of fresh basalts sample were collected to pick up zircons. The rock was dark green in color and had an amygdaloidal structure. The surface of the sample was first washed clean with water and dried naturally. The sample was then crushed to 80 meshes. After coarse washing with water, strong magnetic separation, electromagnetic separation, and fine washing with alcohol, the zircons were hand-picked under a double microscope.
Zircon U-Pb analyses were conducted at the Key Laboratory of Crust-Mantle Materials and Environments, University of Science and Technology of China. U-Pb abundance was measured using the latest Neptune Plus multiple collectors (ICP-MS) from Thermo Fisher Co. Ltd (Waltham, MA, USA). The laser-ablation system used in the measurement was the GeoLasPro 193 nm developed by the Coherent Co. Ltd (Santa Clara, CA, USA). Helium was used as a carrier gas to enhance transport efficiency of ablated material. The spot size of the laser ablation beam was 32 μm. The LA-ICP-MS operating conditions were optimized based on measurements of the reference material zircon 91500. The accuracy of the data was verified by using GJ-1 as an auxiliary standard. The LA-ICP-MS measurement was carried out using time-resolved analysis operated in fast peak-hopping and DUAL detector mode with a short integration time. The Harvard standard zircon 91500 and GJ–1 were measured after every 5 to 10 sample spots, to ensure no drift was occurring. The data were analyzed in the ICPMSDataCal program [28] and the Isoplot program [29].

3.2. Major and Trace Element Analyses

Bulk-rock major and trace element compositions of the samples were measured at the Testing Center of Rock and Mineral in Henan province. The major elements were analyzed using a ZSX100e (Rigaku Co., Akishima, Tokyo, Japan) X-ray fluorescence spectrometer (XRF) on fused glass beads. The trace elements, including rare earth elements, were measured by inductively coupled plasma mass spectrometry (ICP-MS) with an XSERIES2 (Thermo Fisher Co. Ltd, Waltham, MA, USA). A detailed methodology of the analytical procedures can be found in Gao [30]. The analyses of the international standards returned values that agreed with their published values. Analyses of the international rock standards indicated that the precision and accuracy were better than 1.5% for all elements.

3.3. Whole Rock Sr–Nd–Pb Isotopic Analyses

The Sr-Nd isotope analyses were carried out at the Ministry of Education Key Laboratory of Orogenic Belts and Crustal Evolution, Peking University. Powdered bulk-rock samples were first spiked with mixed isotope tracers and then dissolved in a solution of HF and HNO3 in Teflon capsules before undergoing Rb-Sr and Sm-Nd isotope analyses. Rb, Sr, Sm, and Nd were separated using conventional ion exchange procedures, as described by Yan [31]. The Sr-Nd isotopic data were measured on a VG Axiom mass spectrometer. The Nd and Sr ratios were normalized to 146Nd/144Nd = 0.7219 and 86Sr/88Sr = 0.1194, respectively. The BCR-2 standards, which were 143Nd/144Nd = 0.512633 ± 0.000017 (2σ) and 87Sr/86Sr = 0.705013 ± 0.000019 (2σ), respectively, were used to assess analytical precision.
The Pb isotope analyses were tested at the Beijing Institute of Uranium Geology using a Isoprobe-T (GV, Manchester, UK) thermal ionization mass spectrometer (TIMS). These samples were first placed in crucibles and dissolved in HF and HClO4, then the purified Pb was extracted using basic anion exchange resin [32]. Analytical results for the NBS981 standard agreed with the reference value [33].

4. Results

4.1. Zircon U–Pb Dating

The LA–ICP–MS zircon U–Pb dating results are listed in Table 1. The sample ISKB–01 was collected from Qilinshan that was located at 22°19′40″ N, 103°16′43″ E. Twenty-five zircon grains were picked out from sample ISKB–01.
The majority of the zircon grains separated from the sample were light gray in color, euhedral in shape, and transparent in opacity under the microscope (Figure 3a). The grains were 50 to 200 μm long with elongation ratios ranging from 1:1 to 3:1. Almost all of the zircons exhibited oscillatory zoning in CL, implying a magmatic origin. The Th and U concentrations were 36.38 to 669.17 ppm and 71.73 to 721.1 ppm, respectively, with Th/U ratios ranging from 0.86 to 2.75. Twenty-five spots were tested, and all were from a single age group clustered in 256 to 237 Ma; the spots yielded a weighted mean 206Pb/238U age of 244 Ma (MSWD = 4.9) (Figure 3b). This age is considered to represent the crystallization age of the magmatic zircons.

4.2. Whole Rock Geochemistry

Fifty samples were measured for major and trace element analyses (Supplementary Material, Table S1). These samples were collected from Qilinshan and Laochang, respectively. Almost all the samples showed different degrees of alteration with a large variation in loss on ignition (LOI) (1.35–9.08 wt.%), demonstrating relatively strong alteration.
For the samples from Qilinshan, the SiO2 content ranged from 40 to 48.68 wt.%. Most rocks plotted fell in the alkaline basalts field, as seen in Figure 4a,b, and belonged to the potassic and sodic series (Figure 4c). These rocks had high TiO2 contents (2.14–3.23 wt.%), with the TiO2 contents of most samples being larger than 2.5, and belonging to the high-Ti basalts (Figure 4d), as defined by Xu [34]. The MgO contents were 7.76–13.92 wt.% and the Mg# = 53.27–67.77, which is characteristic of primary magma. The TFe2O3 content ranged from 10.18 to 16.06 wt.%. The K2O contents (0.22–2.31 wt.%) in Qilinshan basalts were much lower than that in Laochang basalts. The LILEs were enriched relative to the HFSEs. The (La/Yb)N ratios varied from 8.20 to 23.68 (mean value = 13.34). As revealed by the primitive mantle normalized trace element diagram and the chondrite normalized rare earth element (REE) diagram (Figure 5), the patterns of the Qilinshan basalts were similar to the Emeishan basalts and strongly resembled those of OIB.
The Laochang basalt samples had extremely low SiO2 contents (39.33–44.49 wt.%). Most samples fell in the basanite and basalt areas in Figure 4a, and belonged to high-Ti alkaline basalts in Figure 4b,d. In the diagram showing Na2O vs. K2O, the rocks had high-K characteristics (Figure 4c). The TiO2 content ranged from 2.24 to 3.07 wt.%. The Laochang basalts had higher MgO content (12.16–19.58 wt.%) and Mg# values (64.39–76.95) relative to those of the Qilinshan basalts. The contents of TFe2O3 and K2O were 11.05–14.02 wt.% and 2.12–6.45 wt.%, respectively, for the Laochang basalts. For the trace elements and REEs, the (La/Yb)N ratios varied from 7.43 to 18.96 (mean value = 12.24). These samples exhibited strongly positive Rb anomalies and negative Ba anomalies in the primitive mantle normalized trace element diagram (Figure 5). As can be seen in Figure 5, the patterns of immobile elements in Laochang and Kafang basalts were consistent with those of Emeishan basalts and OIB. Mobile elements such as Rb, Ba, Sr, K, and Pb have high activities and are sensitive to physical and chemical alterations. Therefore, the abnormities of these elements in Laochang and Kafang may have resulted from the process of metamorphism and/or hydrothermal alteration.

4.3. Sr–Nd–Pb Isotopic Geochemistry

Whole-rock Sr-Nd-Pb isotopes of the samples from Qilinshan and Laochang are listed in Table 2 and Table 3. The initial Sr-Nd-Pb isotopic ratios for all the samples were corrected to 244 Ma, according to our new zircon U-Pb dating age. The initial 87Sr/86Sr values of Qilinshan basalts ranged from 0.7044 to 0.7047 with εNd(t) values ranging from 4.69 to 4.92. The Laochang basalts had smaller initial 87Sr/86Sr values (0.7044–0.7048) and εNd(t) values (3.25–3.43). Lead isotopes are more complex because U, Th, and Pb are all mobile during alteration. The initial 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb ratios in Qilinshan basalts were 17.493–18.150, 15.530–15.613, and 37.713–38.853, respectively, and 17.976–18.197, 15.683–15.722, and 38.501–38.713 in Laochang basalts, respectively.

5. Discussion

5.1. Magma Source

In the past decade, the GAAB have attracted a lot of attention for its close relationship with the Cu deposits in the Gejiu ore district [22,36]. However, relatively little research has focused on how the GAAB were formed. For this reason, the magma source of the GAAB remain unresolved. While it is widely accepted that these basalts were the product of the melting of mantle peridotite, the identification of the mantle source has been proven difficult because of the complexity of lithospheric mantle [37]. The Sr-Nd-Pb isotopic characteristics of igneous rocks can often narrow the potential source regions of basalts because isotopic fractionation is not affected by magma crystallization and segregation in the magmatic process. The Sr and Nd isotopic characteristics of the GAAB were consistent, the initial 87Sr/86Sr = 0.7044–0.7048 and 143Nd/144Nd = 0.51249–0.51257, and the Pb isotopes exhibited an appropriate variation range. In the diagram of (87Sr/86Sr)i vs. εNd(t) (Figure 6a), all of the samples fell in the field of the Emeishan flood basalts and showed similarities with the OIB. Moreover, Pb isotopes also showed similar characteristics to Emeishan flood basalts (Figure 6b). The Sr-Nd-Pb isotopic data indicated that the GAAB were derived from the same OIB-like source as the Emeishan flood basalts.
Typically, the ratios of incompatible elements that share similar characteristics in the mantle (such as Zr/Nb and Nb/Th) are not strongly fractionated from each other during the process of partial melting or fractional crystallization. Hence, their ratios can be used to identify the source of magma [39,40]. The Nb/Th ratio is insensitive to various degrees of melting of garnet lherzolite, while the Zr/Nb ratio is moderately affected by different degrees of melting [40]. Therefore, the mantle source can be determined by comparing the Nb/Th and Zr/Nb ratios (Figure 7a). Most of the samples fell in the field near OIB, implying that the GAAB were derived from an enriched mantle sources similar to that of OIB.
Magma sources can also be identified by their Nb/Y and Zr/Y ratios, this is because of their predictability during the partial melting and fractional crystallization processes [41]. Thus, Fitton [42] proposed the formula: δNb = log(Nb/Y) + 1.74 − 1.92 × log(Zr/Y), based on the Nb/Y and Zr/Y ratios. When δNb > 0, the magma is related to an enriched mantle, but when δNb < 0, the magma is related to a depleted mantle. Almost all of the samples had δNb > 0, indicating an enriched mantle source. Likewise, enriched mantle sources can be identified by comparing Zr/Y and Nb/Y (Figure 7b). These comparisons revealed that the majority of the samples fell in the OIB field, indicating the GAAB were derived from enriched mantle.
HFSEs and REEs are immobile during the alteration and weathering processes [43,44,45]. Therefore, the contents and ratios of light REEs and HFSEs are widely used to distinguish between magma sources and determine the degree of partial melting [46,47]. In the diagram showing La/Nb vs. La/Ba (Figure 8a), most samples can be seen to fall in the field of asthenosphere and OIB, with no indicators for crust contamination. Relative to heavy REEs (such as Yb), the enrichment of middle REEs (such as Sm) depends on the presence of garnet in the residual phase during the melting process. Sm is incompatible with garnet, whereas Yb is compatible, this means that the ratio of Sm/Yb can be intensely fractionated when there is a low degree of melting. Accordingly, using Sm vs. Sm/Yb, the degree of partial melting of the mantle source can be constrained using the non-modal batch melting equations [48,49]. Most of the samples had high MgO content (>8 wt.%), which could indicate that the historical source of the basaltic magma underwent partial melting [3]. As can be seen in Figure 8b, the GAAB originated from 5% to 15% partial melting of garnet lherzolite.
Generally, the TiO2 content in magma from the asthenosphere is about 1.27 wt.%, while in magma from deeper mantle material it is generally more than 2 wt.% [37]. The GAAB had high TiO2 content (TiO2 > 2 wt.%), similar to the representative OIB (TiO2 = 2.87 wt.%; [41]), and the Ti/Y ratios ranged from 620 to 1533, similar to the Emeishan high-Ti basalts [34], indicating they derived from the deeper enriched mantle. The OIB-like basalts studied here suggested that there was a period of within plate magmatism in the South China Block around 244 Ma. In the diagram of (87Sr/86Sr)i vs. (143Nd/144Nd)t (Figure 9f), the samples fell near the OIB field and displayed enriched mantle (EM1) evolutionary trends, which indicated they were related to an ancient subcontinental lithospheric mantle (SCLM) metasomatized by a small volume of volatile-enriched melt that originated from asthenosphere or deeper mantle [51,52,53]. As described above, based on the combination of geochemical and isotopic characteristics of the GAAB, it can be concluded that the GAAB were mainly derived from deeper enriched mantle material and experienced 5% to 15% partial melting of garnet lherzolite.

5.2. Petrogenesis

Parental magma compositions are determined by the nature of the mantle source, conditions during mantle melting, fractional crystallization, and the extent of crustal contamination [7]. REEs, HFSEs, and Sr-Nd-Pb isotope compositions are commonly used to estimate these variables for a given sample. Using basaltic magma, the conditions during mantle melting can be investigated to provide information about the processes by which they formed [54]. Although alteration is pervasive in the GAAB, the abundances of compatible and incompatible elements in basaltic melts are not strongly influenced by alteration or weathering [54], so they can still serve as accurate indicators of historical conditions.
A low degree of partial melting of pyrolite can lead to the enrichment of incompatible elements, but with an increasing degree of melting, the enrichment of incompatible elements is reduced. Light REEs and highly incompatible elements are mainly enriched in alkaline basalts with low SiO2 content. Evidence has shown that alkaline basalts are always generated by 2% to 10% partial melting of the incompatible elements enriched mantle source [55,56,57]. The GAAB had trace element compositions and light REEs signatures similar to the OIB. The enrichment of the trace elements and light REEs indicated that the degree of partial melting was less than 10%. This conclusion can also be supported by the diagram of Sm vs. Sm/Yb (Figure 8b).
Fractional crystallization (FC) is integral to magma evolution. Hence, it is always used to interpret geochemical characteristics observed in evolved volcanic rocks. As can be seen in the Nb vs. Zr plot in Figure 9a, the FC process existed. Moreover, the negative correlations that can be observed in the diagrams of CaO/Al2O3 vs. Al2O3 (Figure 9b) and Sc vs. Ti/Y (Figure 9c) implied that the fractionation was of clinopyroxene, which was consistent with the petrographic features. Plagioclase fractionation appeared to be limited as there was no clear evidence for negative Eu anomalies, however most of the samples did have negative Sr anomalies (Figure 5). The near ubiquity of Sr anomalies might be attributed to the alteration or metamorphism during post-magmatic events. The negative correlations between Mg# and TFe2O3 (Figure 9d) and between Mg# and TiO2 (Figure 9e) indicated the fractionation of Ti-Fe oxides. Based on the experimentally determined mantle solidus [40,59,60], magma segregation depth of basalts can be constrained by the CaO/Al2O3 vs. Al2O3 diagram. As seen in Figure 9b, the melts segregation depth of the GAAB was between 2 and 4 GPa (60–120 km).
Crustal contaminated mafic melts have characteristically high initial 87Sr/86Sr ratios, low εNd(t) values, and negative Nb and Ta anomalies [61]. However, the GAAB had relatively low initial 87Sr/86Sr ratios, high εNd(t) values, and no Nb and Ta anomalies (Figure 5), which suggested that the crustal material in the magma was limited. Weak correlations between SiO2 and La/Nb (Figure 10a) and the non-linear relationship between SiO2 and εNd(t) (Figure 10b) also indicated limited crustal contamination. The Nb/U ratio in primary mantle-derived magma is always greater than 47, and the La/Nb and La/Ta ratios are always smaller than 1.5 and 22, respectively. These ratios can be used to identify the existence of crustal material due to their sensitivity to crustal contamination [62,63,64].
The Nb/U ratio in the GAAB was much higher than crustal material, but close to mantle-derived values. Likewise, the smaller La/Ta and La/Nb ratios (La/Ta ≤ 18; La/Nb ≤ 1.46) in most samples revealed similarities with primary magma and also indicated limited crustal contamination. We can determine the existence of crustal material in mantle-derived magma using the diagram of (Th/Ta)PM vs. (La/Nb)PM. As can be seen in Figure 10c, most of the samples fell in the uncontaminated field of the plot, showing there was little or no crustal material in the magma. These signatures indicate that the assimilation of crust during the generation of the basalts was insignificant, and therefore the chemical compositions of these basaltic rocks accurately reflect the characteristics of mantle source regions. Nb/Th and Ti/Yb ratios can be used to identify the lithospheric mantle materials in basalts [66]. In the diagram of Ti/Yb vs. Nb/Th (Figure 10d), most of the samples fell in the field of the OIB and showing evolutionary trends consistent with SCLM. OIB are widely believed to be related to hotspots or mantle plumes, which are usually imaged as columns of heated material ascending from the core-mantle boundary or mantle transition zone [67,68,69,70,71,72]. The upwelling of asthenospheric mantle or asthenospheric melts generated by rift events in an extensional regime can provide enough heat for the melting of the SCLM. In this case, the OIB-like magma mixed with the SCLM magma, which then formed the primary magma of the GAAB and experienced limited crustal contamination during the ascent.

5.3. Tectonic Setting

The tectonic setting of the GAAB is controversial and various viewpoints still receive support. For example, Zhang [21] proposed that the GAAB were generated in an epeiric sea semi-restricted gulf environment, Wang [13] concluded that these basalts were formed in an orogenic environment. The proposed tectonic settings of the GAAB also include within-plate extensional environment [14,15]; back-arc rift basin [16,17,18,19]; and decompressive melting of Emeishan plume head induced by a rift event [20,21]. To clarify the tectonic setting, we provided new zircon dating, major, trace element, and Sr-Nd-Pb isotopic data from these basaltic rocks collected from several representative outcrops and drillholes in the Gejiu ore district.
In Gejiu district, the Gejiu-Napo sedimentary basin has mainly occurred in the Triassic. The lower Triassic Yongningzhen and Feixianguan Formations are composed of shallow water clastic rocks containing fuchsia greywacke and conglomerate. The middle Triassic Gejiu Formation consists mainly of thick-bedded dolomite, limestone, and mudstone. The deposition depth of this sequence deepens gradually upward. The GAAB mainly occurred within the lower section of the Gejiu Formation. The upper Triassic sequence comprises macker and coarse clastic rocks. This sedimentary sequence is characterized by shallow water coarse-grained sediments, complex gravel composition, and coarse gravel sediments from deep to surface. The molasse facies of the sea-land interaction environment marked the shrinkage and closure of the rift basin. The thickness of the Triassic strata (approximately 4000 m) increased dramatically in the Gejiu area [18]. The stratigraphic thickness thinned sharply on both the eastern and western sides of Gejiu (Figure 11). Besides, in Triassic, the bimodal magmatism is also developed in Gejiu district, including the alkaline basalt, dacite, and rhyolite [73]. The geological evidence indicates a rift-related volcanic-sedimentary event. Considering the zonal distribution of the sequence and the variation of stratigraphic thickness, the rift was likely controlled by a syngenetic fault.
Elements such as Ti, Zr, Y, Nb, Hf are useful in distinguishing basalts from different tectonic environments [74,75]. In the diagrams of Nb-Zr-Y (Figure 12a), Ti-Zr-Y (Figure 12b), and Hf-Th-Nb (Figure 12c), the majority of samples are distributed in the field of within-plate settings corresponding to the within-plate alkaline basalts. Moreover, the GAAB had characteristics of enrichment in light REEs, OIB-like geochemical signatures, and was similar to the high-Ti basalts of the ELIP. Young eruption age (244 Ma) excludes the possibility that the GAAB formed during the main event of ELIP (260–257 Ma) [76]. These basalts were coeval and genetically associated with the rift event in this area (Figure 11). Considering the facts described above, we propose that the GAAB erupted within the western margin of the South China Block in an extensional environment that was related to the Gejiu-Napo rift event in the Triassic.
The Ailaoshan suture zone comprises several structurally juxtaposed tectonic units, including the Western Ailaoshan volcanic belts, Ailaoshan ophiolitic melange, Ailaoshan metamorphic complex from west to east [78,79,80,81,82,83,84,85]. Based on the comparison between the Permian and Triassic sedimentary rocks along the Ailaoshan suture zone, Xu [86] proposed they had different detrital provenance and formed in a depositional setting, which was likely caused by the closure of the Ailaoshan Ocean. Both the sedimentology and structural geology evidence show that the Ailaoshan suture zone has been a branch of the Paleo-Tethys Ocean and is the boundary between the South China Block and Indochina Block. The Paleo-Tethys Ailaoshan Ocean subducted beneath the Indochina Block in the Late Permian, and the onset of the collision between South China and Indochina blocks occurred in Early Triassic, around 250 Ma [23]. The Phia Bioc granites (248–245 Ma), Tongtiange leucogranites (~247 Ma), and rhyolites (247–246 Ma) in the Gaoshanzhai, Pantiange and formations are related to syn-collisional crust thickening [87,88,89]. The GAAB with the age of 244 Ma formed in the Gejiu-Napo rift basin were related to a post-collisional setting after the South China-Indochina collision (Figure 13).

5.4. Relationship with the ELIP

Traditionally, the GAAB were considered to be placed in the intermediate zone of the ELIP and most likely formed at the periphery of the ELIP with a low degree of melting of plume material [7,20,34]. Recent studies have suggested there was a post-ELIP magmatism in the period following 260 Ma [20,82]. The Triassic basalts in the southern ELIP have mainly been found in the Kaiyun, Qilinshan, and Laochang-Kafang areas. Based on the methods of geochronology, geochemistry, and Sr-Nd-Pb isotope analyses, Shellnutt [82] thought the magmatism that formed in 252 to 242 Ma in the spatial field of the ELIP was related to the post-ELIP magmatism caused by decompressive melting of the fossil Emeishan plume head beneath the South China crust that was associated with the collision between the South China and North China Blocks during the Middle Triassic. Zhang [20] concluded that, in Gejiu, these basalts were the product of the melting of the plume head after the main ELIP phase caused by the rift system along the southwestern margin of the South China Block during the Early Triassic. Zhang [16], on the other hand, thought there was no relationship between the GAAB and the ELIP because zircon U-Pb dating placed the age in Kafang at 214 Ma. It is noteworthy that the basalts in Kafang and Laochang both underwent intense alteration and metamorphism since their formation because of the extensive metallogenesis during the late Cretaceous tectonomagmatism, which may explain the inaccuracies in dating results.
Although the relationship between the GAAB and the ELIP has been discussed in recent publications [16,20], the GAAB, especially its eruption age, remain relatively understudied. Zhang [21] has reported the SIMS zircon U–Pb age of GAAB in Kafang was 244.4 Ma. The similar LA-ICP-MS U–Pb age of Kaiyuan basalts in adjacent area was 247 Ma [20]. In this study, the zircon U–Pb age reveals that the non-mineralized GAAB in Qilinshan were formed in 244 Ma. Generally, the zircon grains in basalts are small and dark in color. In addition, the existence of oscillatory zoning in zircon grains indicates their magmatic origin. The characteristics of trace elements show that the assimilation of crust in generation of the basalts was insignificant. Besides, the GAAB are interbedded within the Triassic Gejiu Formation, which was considered to be formed in 245 to 237 Ma [21]. Combining with the regional geology, the GAAB and the Gejiu Formation are the important constituents of the volcanic-sedimentary sequence in Middle Triassic in Gejiu area. Thus, we thought the zircon U–Pb age can reflect the magmatic history of the GAAB.
After the formation of the ELIP in ~260 Ma, minor magmatic events occurred around the center of ELIP between 252 to 242 Ma. However, these post-260 Ma magmatic events were not directly related to Emeishan magmatism. This is because most large igneous provinces worldwide had relatively short durations (1–5 Ma). ID-TIMS zircon U–Pb ages show that the Karoo large igneous province in South Africa lasting about 1 Ma or less for the major pulse of magmatism [90,91]. The emplacement of large volumes of volcanic rocks during the main pulse of the Siberian Traps in Russia occurred within <1 Ma [92]. New CA-ID-TIMS U-Pb zircon ages from the Malwa Plateau indicate that the Deccan large igneous province in India erupted from 65.9 to 66.5 Ma [93].
As discussed above, the geochemical characteristics of the GAAB are similar to the Emeishan high-Ti basalts. However, the U-Pb dating age of 244 Ma obtained from Qilinshan basalts in Gejiu reveals a later date than the ELIP (ca. 260 Ma), as constrained by various dating methods in different kinds of rocks [4,27,94]. It is generally accepted that the magmatism in ELIP began at, and ended, shortly after 260 Ma [4,8,82,95,96,97]. Considering the age discrepancies and difference in tectonic setting, there is no geodynamic or genetic link between GAAB and ELIP. The similar geochemical characteristics between the GAAB and the Emeishan high-Ti basalts are most likely due to the similar magma source.

6. Conclusions

Combined with geochronological, petrological, and geochemical studies of the alkaline basalts in the Gejiu area, our conclusions are as follows:
  • Zircon U-Pb dating results showed that the GAAB were formed in 244 Ma (MSWD = 4.9, n = 22).
  • The GAAB, similar to OIB and Emeishan high-Ti basalts, displayed enriched LREE patterns, with LILEs enriched relative to HFSEs. The GAAB had consistent Sr-Nd isotope compositions: the (87Sr/86Sr) = 0.7044–0.7048, and εNd(t) = 3.25–4.92. The Pb isotopes were more complex, the (206Pb/204Pb)t = 17.493–18.197, (207Pb/204Pb)t = 15.530–15.722, (208Pb/204Pb)t = 37.713–38.853, respectively.
  • The GAAB originated from deeper enriched mantle material with 5% to 15% partial melting of garnet lherzolite and a segregation depth between 2 and 4 GPa (60–120 km). During the formation of the GAAB, clinopyroxene and Ti-Fe oxides were fractionally crystallized with insignificant crustal contamination.
  • The GAAB were the product of the decompressive melting of the deeper enriched mantle in a extensional environment that was related to the Gejiu-Napo rift event formed in a post-collisional setting after the South China-Indochina coillision.

Supplementary Materials

The following is available online at https://www.mdpi.com/2075-163X/10/11/1030/s1, Table S1: Data of major and trace elements in this paper.

Author Contributions

Data curation, Z.S.; formal analysis, Z.S.; funding acquisition, Y.C.; investigation, Z.S.; project administration, Y.C.; supervision, Y.C.; writing—original draft, Z.S.; writing—review and editing, Y.C. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the National Natural Science Foundation of China (Grant No. 41972312, 41672329), the National Key Research and Development Project of China (Grant No. 2016YFC0600509), and the Project of China Geological Survey (Grant No. 1212011120341).

Acknowledgments

We are thankful to Guopei Mo, Zhenfei Ma, Lina Zhang, and Luxue Qin for their assistance with samples collection, Shibo Liu for his help with zircon U–Pb dating. We also thank Xiangguo Guo for his help with thin sections observation. We are also indebted to the academic editor and three anonymous reviewers for their critical and constructive comments which substantially improved an early version of the manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. (a) Simplified tectonic map showing the study area in relation to major tectonic units in South China [23], JSJS: Jinshajiang suture, SCS: Song-Chay suture, SMS: Song Ma suture, RRF: Red River fault, DBF: Dien Bien Phu fault; (b) Simplified map showing the location of the study area [27]; (c) Geological map of the Gejiu ore district [21]; (d) Geological section of basalts in Laochang ore segment.
Figure 1. (a) Simplified tectonic map showing the study area in relation to major tectonic units in South China [23], JSJS: Jinshajiang suture, SCS: Song-Chay suture, SMS: Song Ma suture, RRF: Red River fault, DBF: Dien Bien Phu fault; (b) Simplified map showing the location of the study area [27]; (c) Geological map of the Gejiu ore district [21]; (d) Geological section of basalts in Laochang ore segment.
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Figure 2. Typical hand specimen (a,d), single-polarized (b,e), and cross-polarized (c,f) light photomicrographs of basalts in Qilinshan (a–c) and Laochang (d–f). Px—pyroxene, Pl—plagioclase, Hbl—hornblende, Ol—olivine, Bt—biotite, Act—actinolite.
Figure 2. Typical hand specimen (a,d), single-polarized (b,e), and cross-polarized (c,f) light photomicrographs of basalts in Qilinshan (a–c) and Laochang (d–f). Px—pyroxene, Pl—plagioclase, Hbl—hornblende, Ol—olivine, Bt—biotite, Act—actinolite.
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Figure 3. (a) Cathodoluminescence (CL) images of the selected zircons for LA–ICP–MS dating; (b) Concordia diagram of zircon U–Pb age for the Qilinshan basalts.
Figure 3. (a) Cathodoluminescence (CL) images of the selected zircons for LA–ICP–MS dating; (b) Concordia diagram of zircon U–Pb age for the Qilinshan basalts.
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Figure 4. (a): SiO2 vs. Na2O+K2O classification diagram; (b): Nb/Y vs. Zr/Ti diagram; (c): Na2O vs. K2O classification diagram; (d): TiO2 vs. Ti/Y diagram. The data of Kafang from [16].
Figure 4. (a): SiO2 vs. Na2O+K2O classification diagram; (b): Nb/Y vs. Zr/Ti diagram; (c): Na2O vs. K2O classification diagram; (d): TiO2 vs. Ti/Y diagram. The data of Kafang from [16].
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Figure 5. Chondrite normalized REE patterns and primitive mantle normalized trace element patterns of the GAAB. Normalization and OIB values followed [35]. The data of Emeishan basalts from [3]. The data of Kafang from [16].
Figure 5. Chondrite normalized REE patterns and primitive mantle normalized trace element patterns of the GAAB. Normalization and OIB values followed [35]. The data of Emeishan basalts from [3]. The data of Kafang from [16].
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Figure 6. (a) (87Sr/86Sr)i vs. εNd(t) diagram (modified from [3]), OIB: ocean island basalt; (b) (206Pb/204Pb)t vs. (208Pb/204Pb)t diagram (t = 244 Ma, modified from [38]), EM1: enriched mantle 1, EM2: enriched mantle 2, DM: depleted mantle, HIMU: high 238U/204Pb mantle end member, NHRL: northern Hemisphere reference line; data of Emeishan basalts from [27].
Figure 6. (a) (87Sr/86Sr)i vs. εNd(t) diagram (modified from [3]), OIB: ocean island basalt; (b) (206Pb/204Pb)t vs. (208Pb/204Pb)t diagram (t = 244 Ma, modified from [38]), EM1: enriched mantle 1, EM2: enriched mantle 2, DM: depleted mantle, HIMU: high 238U/204Pb mantle end member, NHRL: northern Hemisphere reference line; data of Emeishan basalts from [27].
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Figure 7. Diagram showing mantle components and fields for basalts from various tectonic settings [40,42]. (a) Nb/Th vs. Zr/Nb, SUB: subduction; (b) Zr/Y vs. Nb/Y. NMORB: normal mid ocean ridge basalts, DM: depleted mantle, REC: recycled components, EN: enriched, DEP: depleted components, ARC: arc basalts, OPB: oceanic plateau and island basalts. The data of Kafang from [16].
Figure 7. Diagram showing mantle components and fields for basalts from various tectonic settings [40,42]. (a) Nb/Th vs. Zr/Nb, SUB: subduction; (b) Zr/Y vs. Nb/Y. NMORB: normal mid ocean ridge basalts, DM: depleted mantle, REC: recycled components, EN: enriched, DEP: depleted components, ARC: arc basalts, OPB: oceanic plateau and island basalts. The data of Kafang from [16].
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Figure 8. (a): La/Nb vs. La/Ba diagram (modified from [50]); (b): Sm vs. Sm/Yb diagram (modified from [3]). The data of Kafang from [16].
Figure 8. (a): La/Nb vs. La/Ba diagram (modified from [50]); (b): Sm vs. Sm/Yb diagram (modified from [3]). The data of Kafang from [16].
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Figure 9. (a) Zr vs. Nb diagram (modified from [58]); (b) CaO/Al2O3 vs. Al2O3 diagram (modified from [40]), ol: olivine, cpx: clinopyroxene; (c) Sc vs. Ti/Y diagram (modified from [7]); (d) Mg# vs. TFe2O3 diagram; (e) Mg# vs. TiO2 diagram; (f) (87Sr/86Sr)i vs. (143Nd/144Nd)i (modified from [58]). The data of Kafang from [16].
Figure 9. (a) Zr vs. Nb diagram (modified from [58]); (b) CaO/Al2O3 vs. Al2O3 diagram (modified from [40]), ol: olivine, cpx: clinopyroxene; (c) Sc vs. Ti/Y diagram (modified from [7]); (d) Mg# vs. TFe2O3 diagram; (e) Mg# vs. TiO2 diagram; (f) (87Sr/86Sr)i vs. (143Nd/144Nd)i (modified from [58]). The data of Kafang from [16].
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Figure 10. (a) SiO2 vs. La/Nb diagram; (b) SiO2 vs. εNd(t) diagram; (c) (Th/Ta)PM vs. (La/Nb)PM diagram (modified from [65]); (d) Ti/Yb vs. Nb/Th diagram (modified from [65]), N-MORB: Normal mid ocean ridge basalt, E-MORB: Enriched mid ocean ridge basalt. The data of Kafang from [16,21].
Figure 10. (a) SiO2 vs. La/Nb diagram; (b) SiO2 vs. εNd(t) diagram; (c) (Th/Ta)PM vs. (La/Nb)PM diagram (modified from [65]); (d) Ti/Yb vs. Nb/Th diagram (modified from [65]), N-MORB: Normal mid ocean ridge basalt, E-MORB: Enriched mid ocean ridge basalt. The data of Kafang from [16,21].
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Figure 11. Stratigraphic correlation of the Triassic strata in the western South China block. The sedimentary data are from [3,18,73].
Figure 11. Stratigraphic correlation of the Triassic strata in the western South China block. The sedimentary data are from [3,18,73].
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Figure 12. (a) Nb–Zr–Y diagram (modified from [74]); (b) Ti–Zr–Y diagram (modified from [75]); (c) Hf–Th–Nb diagram (modified from [77]), IAT: Island arc tholeiite, CAB: Calc-alkaline basalt, N-MORB: Normal mid ocean ridge basalt, E-MORB: Enriched mid ocean ridge basalt, WPT: Within plate tholeiite, WPAB: Within plate alkaline basalt. The data of Kafang from [16].
Figure 12. (a) Nb–Zr–Y diagram (modified from [74]); (b) Ti–Zr–Y diagram (modified from [75]); (c) Hf–Th–Nb diagram (modified from [77]), IAT: Island arc tholeiite, CAB: Calc-alkaline basalt, N-MORB: Normal mid ocean ridge basalt, E-MORB: Enriched mid ocean ridge basalt, WPT: Within plate tholeiite, WPAB: Within plate alkaline basalt. The data of Kafang from [16].
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Figure 13. Schematic drawing of the tectonic evolution of the Gejiu-Napo rift event in Ailaoshan post-collisional setting (modified from [23]), SCLM: subcontinental lithospheric mantle.
Figure 13. Schematic drawing of the tectonic evolution of the Gejiu-Napo rift event in Ailaoshan post-collisional setting (modified from [23]), SCLM: subcontinental lithospheric mantle.
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Table
Table 1. U–Pb isotopic compositions for zircon from Qilinshan basalts sample ISKB–01.
Table 1. U–Pb isotopic compositions for zircon from Qilinshan basalts sample ISKB–01.
SpotTh
(ppm)		U
(ppm)		Th/U
Ratio		207Pb/206Pb207Pb/235U206Pb/238U206Pb/238U
Ratio1σRatio1σRatio1σAge1σ
KB1-1198.92184.460.92730750.053430.003160.279530.015680.037980.00069240.34.3
KB1-241.1697.412.36661810.049660.004520.259820.022940.037980.00084240.35.19
KB1-355.46143.072.57969710.050780.00380.270260.019450.038640.00077244.44.77
KB1-4175.69170.820.97228070.057310.003450.308910.017640.039120.00073247.44.52
KB1-5318.8289.820.90909660.053780.002580.297950.013290.040220.00067254.24.14
KB1-648.4279.031.63217680.050290.005140.274250.027290.039590.00094250.35.82
KB1-740.2480.261.99453280.056390.005970.295870.030480.038080.00095240.95.91
KB1-8182.34280.021.53570250.050960.002510.276510.012730.039380.000652494.04
KB1-950.7597.651.92413790.049590.004570.265750.023760.038890.000862465.35
KB1-1037.277.652.08736560.038420.005610.208610.030040.039410.00095249.15.88
KB1-1136.3871.731.97168770.049670.005430.277870.029680.040590.00099256.56.12
KB1-1250.71139.242.74580950.052850.003890.285810.020240.039240.00078248.14.86
KB1-1341.08109.272.65993180.046610.00420.257530.022540.040090.00086253.45.36
KB1-14391.5337.490.86204340.052470.002310.280270.011340.038760.00062245.13.83
KB1-1553.54134.482.51176690.053360.003840.285940.019770.038880.00076245.94.74
KB1-1657.97143.682.47852340.056980.003730.301680.018820.038410.000752434.68
KB1-1750.91130.352.56040070.054590.003770.295120.01950.039220.000762484.72
KB1-1841.8881.051.93529130.041550.00550.216130.028150.037730.00089238.85.56
KB1-19112.931371.21314090.047670.00390.245590.019470.037370.00075236.54.68
KB1-2057.63148.172.57105670.049840.003560.266790.01830.038830.00075245.64.64
KB1-2147.7123.42.58700210.052560.003890.288340.020490.039790.00082251.55.08
KB1-22669.17721.11.07760360.052150.001770.279380.008360.038850.00057245.73.52
KB1-2348.3192.961.92423930.060080.004670.321540.023980.038810.00086245.55.32
KB1-24109.27141.251.29266950.044570.003370.231590.01690.037680.00072238.54.47
KB1-2545.9120.012.6145970.055870.003780.298420.019290.038730.000752454.67
Table
Table 2. Sr–Nd isotopic compositions of Qilinshan and Laochang basalts.
Table 2. Sr–Nd isotopic compositions of Qilinshan and Laochang basalts.
SampleAge(Ma)Rb(ppm)Sr(ppm)87Sr/86Sr(87Sr/86Sr)iSm(ppm)Nd(ppm)143Nd/144Nd(143Nd/144Nd)iεNd(t)
Laochang-01244637292.10.72630.70444.9222.000.512720.512503.43
Laochang-0224471083.00.79050.70485.4624.610.512700.512493.25
Qilinshan-824417395.10.70520.70476.7033.310.512760.512564.69
Qilinshan-924413549.00.70470.70446.5631.070.512780.512574.92
Table
Table 3. Pb isotopic compositions of Qilinshan and Laochang basalts.
Table 3. Pb isotopic compositions of Qilinshan and Laochang basalts.
SampleAge (Ma)206Pb/204Pb207Pb/204Pb208Pb/204Pb(206Pb/204Pb)t(207Pb/204Pb)t(208Pb/204Pb)tΦμTh/U
Laochang-0124418.554 ± 0.00715.701 ± 0.00539.106 ± 0.01418.19715.68338.7130.5859.653.95
Laochang-0224418.658 ± 0.00415.757 ± 0.00439.252 ± 0.00717.97615.72238.5010.5849.753.97
Qilinshan-0824418.780 ± 0.00615.645 ± 0.00639.282 ± 0.01618.15015.61338.8530.5659.523.89
Qilinshan-0924418.859 ± 0.00615.600 ± 0.00539.145 ± 0.01017.49315.53037.7130.5569.423.79
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Shang, Z.; Chen, Y. Zircon U–Pb Geochronology, Geochemistry and Geological Significance of the Anisian Alkaline Basalts in Gejiu District, Yunnan Province. Minerals 2020, 10, 1030. https://doi.org/10.3390/min10111030

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Shang Z, Chen Y. Zircon U–Pb Geochronology, Geochemistry and Geological Significance of the Anisian Alkaline Basalts in Gejiu District, Yunnan Province. Minerals. 2020; 10(11):1030. https://doi.org/10.3390/min10111030

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Shang, Zhi, and Yongqing Chen. 2020. "Zircon U–Pb Geochronology, Geochemistry and Geological Significance of the Anisian Alkaline Basalts in Gejiu District, Yunnan Province" Minerals 10, no. 11: 1030. https://doi.org/10.3390/min10111030

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Shang, Z., & Chen, Y. (2020). Zircon U–Pb Geochronology, Geochemistry and Geological Significance of the Anisian Alkaline Basalts in Gejiu District, Yunnan Province. Minerals, 10(11), 1030. https://doi.org/10.3390/min10111030

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