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Article

Early Jurassic Mafic Intrusions in the Southern Youjiang Basin, SW China: Petrogenesis, Tectonic and Metallogenic Implications

by
Wen Jiang
1,
Quanren Yan
1,*,
Li Deng
1,
Bin Zhou
1,
Zhongjin Xiang
2 and
Wenjing Xia
3
1
College of Earth and Planetary Sciences, University of Chinese Academy of Sciences, Beijing 100049, China
2
Institute of Geology of Chinese Academy of Geological Sciences, Beijing 100037, China
3
Department of Student Affairs, Beihang University, Beijing 100191, China
*
Author to whom correspondence should be addressed.
Minerals 2019, 9(12), 771; https://doi.org/10.3390/min9120771
Submission received: 28 October 2019 / Revised: 7 December 2019 / Accepted: 8 December 2019 / Published: 11 December 2019
(This article belongs to the Special Issue Role of Magmatic Activity in Generation of Ore Deposits)
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Abstract

:
A suite of mafic intrusions, composed of diabase and micro-gabbro outcrops in the Jingxi area of southern Youjiang Basin, SW China. This study conducts geochronological, geochemical, and Sr–Nd isotopic analyses on the mafic intrusions in Jingxi with the aim of determining their petrogenesis, tectonic setting, and metallogenic implications. Zircon U–Pb dating for the mafic intrusions yielded an age of 183 ± 3 Ma (MSWD = 2.3), which is coeval with the Carlin-like gold mineralization in the Youjiang Basin. The mafic intrusions are alkaline in composition and characterized by low TiO2 (1.25–1.87 wt %) contents and low Ti/Y ratios (410–550). They exhibit OIB-like patterns of trace element distribution and they have low (87Sr/86Sr)i ratios of 0.704341 to 0.705677, slightly negative εNd(t) values of −0.30 to −2.16, low La/Ta (11.57–15.66) and La/Nb (0.77–1.06) ratios, with [La/Yb]N = 6.52–10.63. The geochemical characteristics, combined with regional considerations, suggest that the mafic intrusions originated from partial melting of upwelling asthenosphere within the garnet-spinel transition zone, as a result of intracontinental back-arc extension triggered by the steep subduction of the Paleo-Pacific plate beneath the South China Block. Moreover, the new data not only suggest Early Jurassic magma was a possible heat source, but also support a magmatism-related model for the Carlin-like gold mineralization in the Youjiang Basin.

Graphical Abstract

1. Introduction

Mafic magmas originate from the partial melting of the upper mantle, recording the nature of the mantle source. The geochemical composition and crystallization age of mafic rocks, in this regard, can be used to analyze deep geodynamic processes and regional tectonic setting. At the same time, mafic magmas may also carry ore-forming elements and drive ore-forming hydrothermal fluid circulation. Mafic rocks, therefore, can also provide important information to understand regional metallogenesis.
The Youjiang Basin (also known as Nanpanjiang Basin) is located in the southwest margin of the South China Block (SCB), and the sporadically exposed magmatic rocks in the basin are dominated by mafic rocks (Figure 1). Previous studies have focused on the Late Paleozoic-Triassic mafic rocks [1,2,3,4,5,6,7], while the Late Mesozoic magmatic rocks, especially the Jurassic mafic rocks, were rarely reported. Moreover, little attention has been paid to the Late Mesozoic tectonics of the Youjiang Basin, leading to the tectonic setting of the area being unclear [8]. In addition, the Youjiang Basin is known as the “Dian-Qian-Gui Golden Triangle” region, where the Carlin-like gold deposits are widely developed (Figure 1b) [8,9,10,11,12,13,14,15]. The field crosscutting relationships suggest that the Carlin-like gold mineralization took place between Early Jurassic and Late Cretaceous [13,15]. Furthermore, it has been interpreted that the gold mineralization was associated with deep magmatism, either the ore-forming fluid originated from a magmatic source [12,13,16], or the magma heated meteoric water and drove hydrothermal fluid to extract ore-forming elements from sedimentary rocks [9]. However, outcropping igneous rocks that are coeval with the gold mineralization in the Youjiang Basin has rarely been found, and the thermal event for the gold mineralization remains poorly understood [8]. Therefore, the identification and study of a Late Mesozoic mafic rock in the Youjiang Basin should provide significant clues to analyze the Late Mesozoic tectonics and the thermal driver of the Carlin-like gold mineralization in the area.
In this paper, the Early Jurassic mafic intrusions were newly identified in the Jingxi area of the southern Youjiang Basin (western Guangxi Province, SW China). We have conducted a study of LA-ICP-MS zircon U–Pb dating, whole-rock major and trace elements and Sr–Nd isotopes for the mafic intrusions in the Jingxi area. These data are used to constrain their emplacement age and to explore their petrogenesis and tectonic setting, and they probably shed new light on the Late Mesozoic tectonic evolution and the Carlin-like gold mineralization in the Youjiang Basin.

2. Geological Setting and Petrography

The Youjiang Basin is bound by the Mile-Shizhong-Panxian fault to the northwest, Ziyun-Nandan-Du’an fault to the northeast, Pingxiang-Nanning Fault to the southeast, and extends southward to connect with Song Hien Basin in northeastern Vietnam (Figure 1b). The dominantly exposed strata in the Youjiang Basin are Middle-Lower Triassic deep-marine turbidite depositions and isolated Upper Paleozoic shallow-marine carbonate platforms (Figure 1b). A shallow-marine Lower Triassic carbonate platform developed in the northwest margin of the basin, whereas a small amount of Jurassic-Cretaceous terrestrial clastic rocks sporadically occurred in the interior of the basin (Figure 1b and Figure 2) [19,20]. Known magmatic rocks in the Youjiang Basin are scarce. The mainly exposed magmatic rocks are Permian in age and represented by diabases, gabbros, and basalts (269–254 Ma) [1,2,3,4,5]. Middle Triassic basaltic andesites (241 Ma) [6], Late Triassic gabbro-norites (~215 Ma) [7], and minor Late Cretaceous alkaline ultramafic dikes (85–88 Ma) [21], as well as quartz porphyry dikes (95–97Ma) [11] are also exposed in this region. Recently, it has been suggested that the Youjiang Basin was an intracontinental back-arc basin and the sediments of Triassic turbidite deposition in the basin were derived from poorly preserved continental arc associated with the westward subduction of the Paleo-Pacific rather than the hypothesized collisional orogen between the South China and Indochina Blocks [22,23].Moreover, the Permian gabbros in the Babu area of southern Youjiang Basin were linked to the intracontinental back-arc extension related to the westward subduction of the Paleo-Pacific [24].
The mafic intrusions in the Jingxi area of southern Youjiang Basin occur as sills, small stocks, and dikes (Figure 3a), distributing along faults (Figure 2). The mafic intrusions intruded into Devonian and Carboniferous limestones, and the limestones at the contact zone with mafic intrusions are partially metamorphosed to marbles [25]. Although the mafic intrusions in Jingxi are lacking isotopic age, they have been considered to be emplaced in Mesozoic based on the field relationships [25]. The mafic intrusions range in composition from diabase to micro-gabbro. The diabase is the main rock type, and mainly consists of plagioclase (45–50%) and clinopyroxene (35–45%) with typical diabasic texture; ilmenite and titanomagnetite are the main accessory minerals (Figure 3b–d). The micro-gabbro has similar mineral compositions with the diabase. However, compared to the diabase, the micro-gabbro mostly occurs in the center of an intrusion and has relatively coarse-grained mineral crystals, as it is exemplified by the Naba intrusion (Figure 2).

3. Analytical Methods

3.1. Zircon U–Pb Dating

Samples for zircon U–Pb dating are from coarse-grained micro-gabbros, and about 80–100 kg of rocks were collected for zircon separation. Zircon grains were separated using conventional heavy-liquid and magnetic separation techniques. Subsequently, the zircons were mounted in a diameter of 25.4 mm epoxy resin, and the zircon surfaces were polished following the mounting. Photomicrographs of transmitted and reflected light for the zircons, as well as cathodoluminescence (CL) images of the zircons, were taken for identifying the internal structures and selecting suitable positions for U–Pb isotope analysis. Zircon U–Pb isotope ratios dating was conducted at the Key Laboratory of Metallogenesis and Resource Assessment, Institute of Mineral Resources, Chinese Academy of Geological Sciences (CAGS), Beijing, China. The analyses were carried out on a Bruker M90 inductively coupled plasma-mass spectrometry (Bruker, Billerica, MA, USA) that was attached to a Resolution S155 193 nm laser ablation system (LA-ICP-MS). The laser ablation uses a beam diameter of 25 μm. The detailed operating procedures for the laser ablation and the ICP-MS system and the data processing are the same as those described by [26]. The zircon U–Pb dating results are listed in Table 1.

3.2. Whole-Rock Major and Trace Element and Sr–Nd Isotope Measurements

Whole-rock major and trace element analyses were performed at the National Research Center of Geoanalysis, CAGS, Beijing, China. Major element oxides were analyzed using X-ray fluorescence (XRF) with an analytical uncertainty of <0.5%. Besides, FeO (wt %) is determined by wet chemical analysis. Trace elements were determined using Inductively Coupled Plasma Mass Spectrometry (ICP-MS). The analytical uncertainties are 10% when the element abundance is <10 ppm, and around 5% when the element abundance >10 ppm. The major and trace element results are listed in Table 2.
Whole-rock Sr–Nd isotope measurements were taken at State Key Laboratory for Mineral Deposits Research, Nanjing University, Nanjing, China, following the methods similar to [27]. For Sr–Nd isotope analysis, about 150~200 mg of powder (crushed to 200 mesh) for each sample was dissolved and purified. The Sr standard NIST SRM-987 and the Nd standard JNdi-1 were used in this study, yielding an average 87Sr/86Sr ratio of 0.710224 ± 0.000007 (n = 4, 1sd) and 143Nd/144Nd ratio of 0.512106 ± 0.000016 (n = 3, 2sd), respectively. The results of Sr–Nd isotopes are shown in Table 3.

4. Results

4.1. Zircon U–Pb Ages

The sample 17Nb-1 is a coarse-grained micro-gabbro, and 30 zircon grains of the sample has been analyzed. One zircon grain (spot 29) with concordance less than 90% was excluded from the calculation. In the remaining 29 zircon grains, the youngest group of 14 zircon grains yielded a mean 206Pb/238U age of 183 ± 3 Ma (MSWD = 2.3, Figure 4). These 14 zircon grains have Th/U ratios of 0.55–1.19, have oscillatory zones, and show similar morphologies, euhedral, ranging in length from 50 to 100 μm, suggesting magmatic origins (Figure 5). The remaining 15 zircon grains obtained older ages, ranging from 223 Ma to 905 Ma, and they show different morphologies and have a certain degree of roundness (Figure 5) consistent with inherited xenocrysts. Therefore, the youngest age of 183 ± 3 Ma is considered as the best estimate of the crystallization age.

4.2. Whole-Rock Geochemical Data and Sr–Nd Isotopic Compositions

All samples underwent various degrees of alteration, as shown by a relatively high loss on ignition values (LOI, 2.43–4.67 wt %). These rocks have a narrow composition of SiO2 (48.00–53.00 wt %) and MgO (5.32–7.09 wt %) and are characterized by low TiO2 (1.25–1.87 wt %) and Ti/Y ratios (410–550, average = 485). On the Zr/TiO2 vs. Nb/Y diagram, all samples plot in the field of alkaline series (Figure 6). The mafic rocks show relatively steep REE patterns (Figure 7a), with (La/Yb)N = 6.52–10.63. On the trace element spider diagram, they show enrichment in incompatible elements (e.g., Rb, Th, and U) similar to OIB, except for higher Ba content (Figure 7b).
The mafic rocks in the Jingxi area have a narrow composition of Sr–Nd isotopes (Table 3). The initial isotopic ratios were calculated to 183 Ma. The (87Sr/86Sr)i ratios range from 0.704341 to 0.705677, and the εNd(t) values range from −0.30 to −2.16. In the (87Sr/86Sr)i versus εNd(t) correlation diagram, they show Sr–Nd isotopic compositions similar to those of OIBs and fall into the field of Early Jurassic mafic rocks in the inland of the South China Block (Figure 8).

5. Discussion

5.1. Petrogenesis

5.1.1. Effect of Alteration, Crustal Contamination, and Fractional Crystallization

The samples of mafic intrusions in Jingxi have a relatively high LOI (2.43–4.67 wt %, Table 2), and therefore it is necessary to evaluate the potential effects of alteration processes on the use of trace elements. In general, Zr is considered as the most immobile element in the low-grade alteration and metamorphism process [40]. Thus, Zr can be used as an alternation-independent index to evaluate the mobility of other elements [41,42]. The high field strength elements (HFSE, e.g., Nb, Ta, Hf, and Ti), REE, Y, Th, and U are significantly correlated with Zr (online Supplementary File, Figure S1), which suggests that these elements were basically immobile during the alteration [42]. It is also supported by the uniform variations of these trace elements (HSFE, REE, Y, Th, and U) on the trace element spider diagram (Figure 7). Therefore, alteration had an insignificant effect on the HFSE, REE, Y, Th, and U of the samples, and the following discussions mainly focus on these immobile elements.
For the mafic intrusions in Jingxi, the inherited zircons and slightly enriched Sr–Nd isotopic compositions imply some degree of crustal contamination. However, the lack of clear correlation between Nb/La and SiO2, MgO (Figure 9a,b) argues against extensive crustal contamination, since crust contamination would decrease Nb/La ratios, resulting in a negative correlation between Nb/La ratios and SiO2, and a positive correlation between Nb/La ratios and MgO. Moreover, the Sr–Nd isotopic compositions for the samples do not clearly correlate with increasing SiO2 and decreasing MgO contents (Figure 9c,d), suggesting insignificant crustal contamination. They have much lower Th/Nb (0.06–0.12) and Th/Ce (0.02–0.06) ratios, but a much higher Nb/U (25.5–36.08) ratio than the upper continental crust (Th/Nb = 0.86, Th/Ce = 0.17, Nb/U = 4.4, [43]. These geochemical signatures are inconsistent with extensive crustal contamination. Thus, we suggest that crustal contamination played an insignificant role during magma ascent, and the enriched Sr–Nd isotopic signatures mainly resulted from source enrichment.
All the basaltic magmas from the Jingxi mafic intrusions are not primary mantle melt as shown by their low Mg# (0.58–0.67), MgO (5.32–7.06 wt %), Ni (17.2–120 ppm), and Cr (53.4–313 ppm) contents. These characteristics suggest that they have experienced a variable degree of fractional crystallization from parent magmas. The negative correlations of MgO, TFe2O3, CaO, and Al2O3 vs. SiO2, and negative correlations of Cr and Ni contents vs. MgO (Figure 10), presumably imply the fractionation of olivine and/or clinopyroxene. In contrast, they show an increase of P2O5 and TiO2 with the increasing SiO2 (Figure 10e,f), which might reflect insignificant fractionation of apatite and Ti–Fe oxides. The weakly positive Eu anomaly (δEu = 1.01–1.12) probably suggests minor accumulation of plagioclase.

5.1.2. Origin of the Mafic Intrusions in Jingxi

The mafic intrusions in Jingxi have intraplate-like low La/Ta (11.57–14.21), La/Nb (0.77–1.06), Zr/Nb (5.72–6.43), and Th/La (0.11–0.18) ratios and high Nb/U (25.50–36.08) ratios, and these ratios fall near or within the range of OIB [29,44,45]. Moreover, they exhibit REE and trace element patterns similar to OIB (Figure 7). The low (87Sr/86Sr)i ratios (0.704341–0.705677) and slightly negative εNd(t) values (−0.30 to −2.16) of the Jingxi mafic rocks probably suggest that they derived from a weakly enriched mantle source. They show low La/Ta ratios (11.57–15.66, i.e., <30) and La/Nb ratios (0.77–1.06, i.e., <1.5) similar to the values observed from the asthenospheric mantle and much lower than those basalts from the lithospheric mantle [46,47], which suggests that they resulted from an asthenospheric mantle. Generally, high [La/Yb]N ratios reflect mantle melting dominated by relatively small melting fractions and/or garnet as the predominant residual phase (thick lithosphere), whereas low [La/Yb]N ratios correspond to larger melting fractions and/or spinel control (thin lithosphere, [48]). The Jingxi mafic intrusions show low [La/Yb]N ratios (6.52–10.63), which implies the spinel is a residual phase. The plot of Sm/Yb vs. La/Sm can effectively distinguish between the melting of spinel-and garnet-lherzolite sources. When a spinel-lherzolite undergoes partial melting, Sm/Yb ratios of the melt are nearly unfractionated, while La/Sm ratios decrease with increasing degree of partial melting. In contrast, Sm/Yb ratios will strongly fractionate during the small (or moderate) degree of partial melting of a garnet-lherzolite source [49,50]. Therefore, partial melting of a spinel-lherzolite source will generate a nearly horizontal melting trend, while a partial melting of a garnet-lherzolite source will create a steep melting trend to higher Sm/Yb ratios on the Sm/Yb against La/Sm plot [49]. The mafic rocks in Jingxi have a steep Sm/Yb melting trend but fall below the garnet-lherzolite melting curves (Figure. 11), and the Sm/Yb-La/Sm systematics also cannot be explained by the partial melting of a spinel-lherzolite source. Thus, the simplest model to explain the Sm/Yb-La/Sm systematics of the mafic rocks in Jingxi is the partial melting of lherzolite in the garnet-spinel transition zone. Furthermore, Figure 11 shows a 3–6% non-model batch melting of a hypothetical light REE-enriched garnet-spinel lherzolite ([La/Yb]N > 1) can generate the Sm/Yb-La/Sm systematics of the Jingxi mafic rocks.

5.2. Tectonic Implications

The OIB-like mafic rocks are usually linked to mantle plume [31,53] or tectonic extension of the continental lithosphere, and the latter may include: (1) lithospheric delamination triggered by gravity instability during post-orogenic stage [54,55]; and (2) intracontinental back-arc extension [30,56]. Zircon U–Pb isotopic data indicate that the mafic intrusions in Jingxi emplaced at 183 ± 3 Ma (Figure 4), which is consistent with the newly reported zircon U–Pb age of Badu diabase in the middle Youjiang Basin (187 ± 3 Ma [57], suggesting that Early Jurassic magmatism occurred in this region. In SW China, the mantle plume activity took place in Middle Permian (Emeishan plume, ~260 Ma, [58,59]), and therefore the Early Jurassic mafic rocks in Jingxi cannot be associated with the Emeishan mantle plume due to the large age gap. A post-orogenic lithospheric delamination tectonic setting would trigger widespread magmatism of diverse compositions, including basaltic rocks with intraplate geochemical characteristics, bimodal magmatism and A-type granites [55,60,61]. However, the delamination mechanism can be excluded due to the limited magmatism and the lack of contemporaneous granitic rocks in the Youjiang Basin and adjacent areas during Early Jurassic. Instead, the mafic rocks in Jingxi exhibit REE patterns and trace spider diagrams similar to the modern back-arc basalts in the Andes (Figure 7), and they are also plotted in the back-arc field on the tectonic discrimination diagrams (Figure 12). Therefore, the mafic intrusions in Jingxi most likely formed at an intracontinental back-arc tectonic setting analogous to the modern Andean back-arc basalts.
It has been suggested that the subduction of the Paleo-Pacific plate beneath the South China Block occurred from the Permian [66,67], and the Permian gabbros in the Badu area of southern Youjiang Basin were linked to the back-arc extension [24]. Additionally, the Youjiang Basin is thought to be an extensional continental back-arc basin associated with the westward subduction of the Paleo-Pacific during Triassic [22,23]. The newly drilled Early Jurassic arc-related granites and diorites from NE South China Sea and SW East China Sea [68,69], combined with Talun granite in SE Taiwan [70], define a NE-SW trending Dongsha-Talun-Yandang magmatic arc zone along the eastern margin of the SCB [68,69]. The identified Jurassic accretionary complexes in Southwest Japan, the Ryukyu Islands, Taiwan, and West Philippines [71,72,73,74] are paired with this magmatic arc zone in response to the subduction of the Paleo-Pacific slab beneath the SCB [68]. In this case, a corresponding back-arc extension regime probably occurred in the inland Youjiang Basin during the Early Jurassic. Accordingly, the Jingxi mafic intrusions show OIB-like trace elements characteristics and have an intracontinental back-arc extensional setting, which is consistent with such a geodynamic model. Therefore, we suggest that the Youjiang Basin was under the tectonic setting of intracontinental back-arc extension caused by the steep subduction of the Paleo-Pacific plate beneath the SCB during the Early Jurassic (Figure 13).

5.3. Implications for the Carlin-like Gold Mineralization in the Youjiang Basin

Although the exact age of the Carlin-like gold mineralization in the Youjiang Basin remains controversial as the age of the gold mineralization is difficult to date directly, the proposed age based on field crosscutting relationships is thought to be the most reliable [13,15]. Some of the orebodies in the Shuiyingdong and Jingfeng gold deposits crosscut the folds consisted of Early Jurassic strata [13,15], while some of the orebodies in the Liaotun gold deposit were crosscut by Late Cretaceous (ca. 95 Ma) felsic dikes (Figure 1b, [11]). These field relationships indicate that the Carlin-like gold deposits in the Youjiang Basin formed between Early Jurassic and Late Cretaceous [13]. Consistent with these crosscutting relationships, various hydrothermal minerals isotopic dating data constrain the age of the gold mineralization to a wide range between 193 Ma and 141 Ma [10,18,75,76]. As mentioned above, the gold mineralization in the Youjiang Basin has long been considered to be related to the deep magmatism, either the ore-forming elements derived from magma or the ore-forming hydrothermal fluid was driven by magma [9,12,13,16]. However, no contemporaneous igneous outcrops in the Youjiang Basin have been found before. Our newly identified Early Jurassic mafic intrusions in the Jingxi area emplaced at 183 ± 3 Ma, which is contemporaneous with the time of the gold mineralization. Such Early Jurassic magma was a probable heat source to drive hydrothermal fluids for the generation of the Carlin-like gold deposits, and it supports the magmatism-related metallogenic model [9,12,13,16]. In addition, the Early Jurassic magmatism in the southern Youjiang Basin was formed at an intracontinental back-arc extensional setting. Therefore, we propose that the metallogenic setting of the Carlin-like gold deposits in the Youjiang Basin is the same intracontinental back-arc extensional regime (Figure 13), which is analogous to Carlin-type gold deposits in Nevada [77,78].

6. Conclusions

(1)
The mafic intrusions in the Jingxi area emplaced at 183 ± 3 Ma, which suggests the discovery of an Early Jurassic magmatic event in the southern Youjiang Basin.
(2)
The mafic intrusions in the Jingxi area have OIB-like geochemical characteristics, and magmas of these mafic rocks derived from partial melting of upwelling asthenosphere within the garnet-spinel transition zone, were as a result of the intracontinental back-arc extension caused by the steep subduction of the Paleo-Pacific plate beneath the South China Block.
(3)
Early Jurassic magmatism was a probable heat source for the formation of the Carlin-like gold deposits in the Youjiang Basin, and it supported a metallogenic setting of intracontinental back-arc extension and a magmatism-related metallogenic model.

Supplementary Materials

The following are available online at https://www.mdpi.com/2075-163X/9/12/771/s1, Figure S1: Elements versus Zr correlation diagrams for mafic intrusions in the Jingxi area, SW China.

Author Contributions

Conceptualization, W.J. and Q.Y.; investigation, W.J., L.D., B.Z., and Q.Y.; writing—original draft preparation, W.J.; writing—review and editing, W.J., Q.Y., L.D., and W.X.; funding acquisition, Q.Y. and Z.X.

Funding

This study was financially supported by the National Natural Science Foundation of China (Grant 40872147) and the China Geological Survey (Grants 12120113067500, DD20160201-07).

Acknowledgments

We are grateful to Zhan Xu of the Yunnan Institute of Geological Survey for the assistance of field geological investigation and to Huanlin Lei of the Nanjing University for the assistance of Sr–Nd isotope analysis.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. (a) Tectonic framework of East Asia (revised after [17]). (b) Simplified regional geological map of the Youjiang Basin and adjacent areas (after [10,18]) and 1:500,000 geological map of central South China made by the Chinese Academy of Geological Sciences in 2012). YJB = Youjiang Basin.
Figure 1. (a) Tectonic framework of East Asia (revised after [17]). (b) Simplified regional geological map of the Youjiang Basin and adjacent areas (after [10,18]) and 1:500,000 geological map of central South China made by the Chinese Academy of Geological Sciences in 2012). YJB = Youjiang Basin.
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Figure 2. Simplified geological map of the Jingxi area (after 1:200,000 geologic map of the Jingxi sheet [25]).
Figure 2. Simplified geological map of the Jingxi area (after 1:200,000 geologic map of the Jingxi sheet [25]).
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Figure 3. Photographs of field outcrop (a) and hand specimen (b) for the representative diabases in Jingxi. Photomicrographs showing petrographic and textural characteristics of the diabase in Jingxi (c,d). Cpx = clinopyroxene; Pl = plagioclase; Ilm = Ilmenite.
Figure 3. Photographs of field outcrop (a) and hand specimen (b) for the representative diabases in Jingxi. Photomicrographs showing petrographic and textural characteristics of the diabase in Jingxi (c,d). Cpx = clinopyroxene; Pl = plagioclase; Ilm = Ilmenite.
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Figure 4. Zircon U–Pb age Concordia plots of the mafic intrusions in Jingxi.
Figure 4. Zircon U–Pb age Concordia plots of the mafic intrusions in Jingxi.
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Figure 5. Cathodoluminescence (CL) images of representative zircons for the mafic intrusions in Jingxi.
Figure 5. Cathodoluminescence (CL) images of representative zircons for the mafic intrusions in Jingxi.
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Figure 6. Geochemical classification of the mafic intrusions in Jingxi. The Nb/Y vs. Zr/TiO2 × 0.0001 diagram from [28].
Figure 6. Geochemical classification of the mafic intrusions in Jingxi. The Nb/Y vs. Zr/TiO2 × 0.0001 diagram from [28].
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Figure 7. Chondrite normalized REE patterns (a), and primitive-mantle normalized trace spider diagrams (b) for the mafic intrusions in Jingxi. Normalizing values and OIB, MORB data are from [29] Andean back-arc basalts are from [30].
Figure 7. Chondrite normalized REE patterns (a), and primitive-mantle normalized trace spider diagrams (b) for the mafic intrusions in Jingxi. Normalizing values and OIB, MORB data are from [29] Andean back-arc basalts are from [30].
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Figure 8. εNd(t) vs.(87Sr/86Sr)i diagram for the mafic intrusions in Jingxi. Data sources: OIB [31], EM Ι (Enriched mantle Ι) & EM II (Enriched mantle II) [32], MORB [33]. The Early Jurassic rocks in the inland of the South China Block are shown for comparison, data sources: [34,35,36,37,38,39].
Figure 8. εNd(t) vs.(87Sr/86Sr)i diagram for the mafic intrusions in Jingxi. Data sources: OIB [31], EM Ι (Enriched mantle Ι) & EM II (Enriched mantle II) [32], MORB [33]. The Early Jurassic rocks in the inland of the South China Block are shown for comparison, data sources: [34,35,36,37,38,39].
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Figure 9. Plots of the mafic intrusions in Jingxi. (a) SiO2 vs. Nb/La; (b) MgO vs. Nb/La; (c) SiO2 vs. (87Sr/86Sr)i; (d) SiO2 vs. (143Nd/144Nd)i. All major oxides are normalized to 100% on a volatile-free basis.
Figure 9. Plots of the mafic intrusions in Jingxi. (a) SiO2 vs. Nb/La; (b) MgO vs. Nb/La; (c) SiO2 vs. (87Sr/86Sr)i; (d) SiO2 vs. (143Nd/144Nd)i. All major oxides are normalized to 100% on a volatile-free basis.
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Figure 10. Harker diagrams for the mafic intrusion in Jingxi. (a) SiO2 vs. MgO; (b) SiO2 vs. CaO; (c) SiO2 vs. Al2O3; (d) SiO2 vs. TFe2O3 (Total Fe); (e) SiO2 vs.TiO2; (f) SiO2 vs. P2O5; (g) MgO vs. Ni; (h) MgO vs. Cr. All major oxides are normalized to 100% on a volatile-free basis.
Figure 10. Harker diagrams for the mafic intrusion in Jingxi. (a) SiO2 vs. MgO; (b) SiO2 vs. CaO; (c) SiO2 vs. Al2O3; (d) SiO2 vs. TFe2O3 (Total Fe); (e) SiO2 vs.TiO2; (f) SiO2 vs. P2O5; (g) MgO vs. Ni; (h) MgO vs. Cr. All major oxides are normalized to 100% on a volatile-free basis.
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Figure 11. A plot of Sm/Yb vs. La/Sm for the mafic intrusions in Jingxi. The shown melt curve of spinel lherzolite and garnet lherzolite are calculated using non-modal batch melting equations of [51]. Numbers along melting curves are the degree of partial melting. Spinel- and garnet-lherzolite models are from [52]. Partition coefficients are taken from the GERM Partition Coefficient Database.
Figure 11. A plot of Sm/Yb vs. La/Sm for the mafic intrusions in Jingxi. The shown melt curve of spinel lherzolite and garnet lherzolite are calculated using non-modal batch melting equations of [51]. Numbers along melting curves are the degree of partial melting. Spinel- and garnet-lherzolite models are from [52]. Partition coefficients are taken from the GERM Partition Coefficient Database.
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Figure 12. Tectonic discrimination diagrams for the mafic intrusions in Jingxi. (a) Y vs. La/Nb [62]; (b) TFe2O3 vs. TiO2 [63]; (c) Zr vs. V/Ti [64]; (d) Ti/1000 vs.V [65]. Andean back-arc basalts are from [30]. BABB = Back-arc basin basalt; FAB = Fore-arc basalt; IAB = Island arc basalt; IAT = Island arc tholeiites; OFB = Ocean floor basalt.
Figure 12. Tectonic discrimination diagrams for the mafic intrusions in Jingxi. (a) Y vs. La/Nb [62]; (b) TFe2O3 vs. TiO2 [63]; (c) Zr vs. V/Ti [64]; (d) Ti/1000 vs.V [65]. Andean back-arc basalts are from [30]. BABB = Back-arc basin basalt; FAB = Fore-arc basalt; IAB = Island arc basalt; IAT = Island arc tholeiites; OFB = Ocean floor basalt.
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Figure 13. Tectonic model for the intracontinental back-arc extensional origin of the Jingxi mafic intrusions and the formation of the Carlin-like gold deposits in the Youjiang Basin, SW China. YJB = Youjiang Basin.
Figure 13. Tectonic model for the intracontinental back-arc extensional origin of the Jingxi mafic intrusions and the formation of the Carlin-like gold deposits in the Youjiang Basin, SW China. YJB = Youjiang Basin.
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Table
Table 1. LA-ICP-MS Zircon U–Pb dating results of the mafic intrusions in Jingxi.
Table 1. LA-ICP-MS Zircon U–Pb dating results of the mafic intrusions in Jingxi.
Spot UPbTh/U207Pb/235U206Pb/238UAge (Ma)Con %
ppmppmRatio1σRatio1σ207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ
17Nb-1, micro-gabbro
01568990.770.20830.00730.02930.0004264.977.8192.16.2186.42.696
02139280.990.21170.01100.02840.0005376.0109195.09.2180.53.392
03357620.840.20400.00680.02780.0004361.277.8188.55.8176.92.793
04204420.980.20900.01190.02780.0005383.4120192.710.0177.13.391
05211481.200.19820.00900.02870.0005205.698.1183.67.7182.63.199
06439900.770.26750.01100.03470.0006431.575.9240.78.8220.13.591
107456470.320.26020.00760.03620.0005294.559.3234.96.1229.03.497
08121230.470.43190.01620.05300.0008576.076.8364.511.5333.24.991
098631190.630.21540.00590.02980.0005298.245.4198.14.9189.53.295
10118170.740.21200.01220.02860.0005350.1126195.210.2181.92.892
117691200.910.18870.00420.02780.0004161.243.5175.53.6176.92.699
126101091.190.21490.01120.02880.0006301.994.4197.79.4182.83.892
13200360.530.34160.01150.04740.0008294.565.7298.48.7298.55.099
14341620.570.33500.00810.04540.0007346.451.8293.46.2286.44.497
15395480.450.24850.00720.03520.0005257.570.4225.35.8223.13.499
165431210.980.22030.00650.02920.0006279.790.7202.15.4185.93.791
17507670.550.20800.00670.02960.0006105.690.7191.85.6187.83.597
189151480.670.21110.00950.02820.0009211.2111194.48.0179.25.691
197671681.040.20790.00540.02990.0005200.173.1191.84.6190.12.999
208531350.740.20730.00450.02900.0005294.546.3191.33.8184.22.896
213681930.960.60430.01460.07810.0013477.844.4479.99.3484.57.699
222621190.700.69180.01480.08560.0013550.040.7533.98.9529.77.799
23238960.810.53850.01610.06720.0011600.059.3437.410.6419.26.495
24116510.321.42410.03450.15060.0021892.348.1899.114.5904.511.699
25159520.930.34920.01130.04750.0008353.870.4304.18.5299.34.698
265301630.850.40250.01200.05140.0008479.783.3343.58.7323.15.293
274832180.421.30830.02730.13210.0021977.531.5849.412.0799.711.993
28194651.050.31410.01160.04460.0008255.679.6277.39.0281.64.998
2913794901.000.41940.00920.05010.0007620.435.2355.66.6315.14.587
302031280.661.15980.02510.12710.0017809.340.7781.911.8771.59.598
Con = Concordance.
Table
Table 2. Whole-rock major (wt %) and trace element (μg/g) of the mafic intrusions in Jingxi.
Table 2. Whole-rock major (wt %) and trace element (μg/g) of the mafic intrusions in Jingxi.
Sample17Lb-117Lb-217Lb-317Lb-417Lb-517Lb-617Lb-717Nb-117Nb-217Nb-317Nb-417Nb-5
SiO248.62 48.00 47.56 47.54 48.35 48.58 48.19 51.11 53.00 50.94 52.96 51.14
Al2O316.38 16.70 16.90 16.65 16.59 16.26 16.59 16.67 15.39 16.32 15.32 16.67
CaO8.27 9.01 9.28 9.72 9.51 10.21 9.06 7.50 4.14 7.57 4.15 7.52
Fe2O32.08 1.75 1.34 1.82 2.15 1.92 2.39 1.71 2.82 2.28 2.45 1.66
FeO6.59 5.80 6.30 5.95 5.30 6.27 5.41 5.73 6.83 5.19 6.74 5.80
K2O1.35 0.75 0.84 0.85 0.70 0.26 0.61 2.14 2.50 2.20 2.50 2.13
MgO7.09 5.57 5.41 5.80 5.87 7.06 5.96 5.82 5.33 5.63 5.32 5.82
MnO0.13 0.13 0.13 0.13 0.12 0.12 0.12 0.12 0.11 0.11 0.11 0.12
Na2O3.94 4.91 4.76 4.47 4.84 4.05 4.73 4.02 5.00 3.98 5.03 4.04
P2O50.22 0.26 0.25 0.24 0.22 0.23 0.22 0.25 0.38 0.28 0.38 0.26
TiO21.30 1.28 1.33 1.39 1.25 1.37 1.29 1.30 1.87 1.41 1.86 1.30
LOI3.02 4.52 4.55 4.56 4.67 3.09 4.43 2.61 2.48 2.76 2.43 2.58
Total98.99 98.68 98.65 99.12 99.57 99.42 99.00 98.98 99.85 98.67 99.25 99.04
Mg#0.66 0.63 0.61 0.64 0.67 0.67 0.66 0.65 0.58 0.66 0.59 0.64
La13.00 17.00 15.90 14.10 14.00 16.60 16.10 16.60 27.70 18.90 28.50 16.30
Ce25.40 31.80 30.50 27.70 27.10 29.40 28.30 31.40 56.60 35.70 57.00 31.40
Pr3.49 4.38 4.12 3.75 3.60 4.71 4.08 4.17 6.95 4.70 7.03 4.10
Nd14.80 18.00 17.00 15.20 14.50 19.60 17.20 17.00 26.30 18.80 26.90 16.80
Sm3.31 3.88 3.57 3.42 3.21 4.41 3.77 3.66 5.61 4.02 5.74 3.62
Eu1.26 1.45 1.42 1.30 1.26 1.67 1.48 1.39 1.89 1.50 1.98 1.38
Gd3.88 4.40 4.07 3.77 3.66 5.16 4.31 4.12 6.11 4.55 6.26 4.10
Tb0.57 0.66 0.62 0.57 0.56 0.75 0.65 0.61 0.89 0.66 0.91 0.61
Dy3.18 3.58 3.36 3.13 3.15 4.25 3.53 3.25 4.69 3.60 4.81 3.29
Ho0.68 0.75 0.69 0.64 0.65 0.88 0.73 0.66 0.96 0.74 1.00 0.66
Er1.77 1.89 1.76 1.66 1.61 2.13 1.86 1.66 2.41 1.84 2.44 1.65
Tm0.25 0.27 0.25 0.24 0.24 0.29 0.27 0.23 0.32 0.25 0.33 0.23
Yb1.43 1.52 1.42 1.33 1.36 1.56 1.48 1.28 1.87 1.42 1.97 1.27
Lu0.23 0.25 0.24 0.22 0.23 0.26 0.24 0.21 0.30 0.24 0.32 0.21
Y14.50 16.90 15.20 14.50 15.10 19.40 16.80 15.30 21.30 16.80 21.10 14.90
Sc20.20 19.50 19.10 20.50 21.20 27.30 22.00 18.50 17.50 19.20 17.30 18.10
V172 151 161 174 146 194 158 161166 163 170 159
Co34.20 29.70 32.00 32.40 30.70 36.90 30.30 29.50 24.70 29.30 25.50 28.50
Ni86.40 126 109 111 119 120 136 60.30 17.20 60 17.40 60.20
Cu57.20 66.00 69.40 66.90 65.20 87.90 80.20 29.00 16.50 35.90 17.30 25.90
Rb19.70 14.80 16.20 17.00 13.60 4.63 12.40 24.80 27.00 25.30 27.00 24.80
Sr628 752 794 758 686 695 652 1038 346 1043 344 1010
Zr85.70 121 123 109 112 101 113 108 175 121 179 109
Nb14.10 19.90 19.90 18.40 18.00 15.70 18.80 18.20 30.60 20.60 31.60 18.00
Ta0.96 1.34 1.34 1.21 1.21 1.06 1.25 1.21 1.99 1.33 2.05 1.22
Ba307 593 695 481 496 544 470 445 485 452 488 447
Hf2.47 3.10 3.04 2.89 2.88 2.65 2.92 2.85 4.41 3.17 4.60 2.82
Pb2.92 2.20 5.38 2.19 1.63 2.72 2.01 2.00 3.60 3.78 3.62 2.02
Th2.08 2.40 2.27 2.00 2.17 1.79 2.18 2.87 4.96 3.23 5.07 2.90
U0.47 0.61 0.58 0.51 0.56 0.46 0.55 0.68 1.20 0.77 1.21 0.70
Cr231 217 196 262 280401 303 292 53.40 313 54 288
La/Ta13.54 12.69 11.87 11.65 11.57 15.66 12.88 13.72 13.92 14.21 13.90 13.36
La/Nb0.92 0.85 0.80 0.77 0.78 1.06 0.86 0.91 0.91 0.92 0.90 0.91
Zr/Nb6.08 6.08 6.18 5.92 6.22 6.43 6.01 5.93 5.72 5.87 5.66 6.06
Th/La0.16 0.14 0.14 0.14 0.16 0.11 0.14 0.17 0.18 0.17 0.18 0.18
Nb/U30.00 32.62 34.31 36.08 32.14 34.13 34.18 26.76 25.50 26.75 26.12 25.71
Ti/Y518 433 513 550 479 410 460 485 488 471 512 501
[La/Yb]N6.528.028.037.607.387.637.809.3010.639.5510.389.21
LOI = loss on ignition. Mg# = Mg2+ / (Mg2+ + Fe2+). [La/Yb]N = La/Yb ratio is normalized to chondritic values.
Table
Table 3. Sr and Nd isotopic compositions of mafic intrusions in Jingxi.
Table 3. Sr and Nd isotopic compositions of mafic intrusions in Jingxi.
SampleAge (Ma)Rb (ppm)Sr (ppm)87Rb/86Sr87Sr/86Sr±1σ(87Sr/86Sr)iSm (ppm)Nd (ppm)147Sm/144Nd143Nd/144Nd±1σ(143Nd/144Nd)iεNd(t)
17Lb-1183 19.7 628.0 0.09080.7059145 0.705677 3.3114.80.1352 0.512549 20.512387 −0.30
17-Lb2183 14.8 752.0 0.05700.7058088 0.705660 3.88180.1303 0.512528 20.512372 −0.59
17Nb-1183 24.8 1038.0 0.06920.7051806 0.705000 3.66170.1302 0.512448 30.512292 −2.16
17Nb-2183 27.0 346.0 0.22600.7049296 0.704341 5.6126.30.1290 0.512450 20.512295 −2.09

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Jiang, W.; Yan, Q.; Deng, L.; Zhou, B.; Xiang, Z.; Xia, W. Early Jurassic Mafic Intrusions in the Southern Youjiang Basin, SW China: Petrogenesis, Tectonic and Metallogenic Implications. Minerals 2019, 9, 771. https://doi.org/10.3390/min9120771

AMA Style

Jiang W, Yan Q, Deng L, Zhou B, Xiang Z, Xia W. Early Jurassic Mafic Intrusions in the Southern Youjiang Basin, SW China: Petrogenesis, Tectonic and Metallogenic Implications. Minerals. 2019; 9(12):771. https://doi.org/10.3390/min9120771

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Jiang, Wen, Quanren Yan, Li Deng, Bin Zhou, Zhongjin Xiang, and Wenjing Xia. 2019. "Early Jurassic Mafic Intrusions in the Southern Youjiang Basin, SW China: Petrogenesis, Tectonic and Metallogenic Implications" Minerals 9, no. 12: 771. https://doi.org/10.3390/min9120771

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