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Article

Geochemical Characteristics and Geological Significance of the Shangsu Mafic Dikes in Jiangxi

by
Yang Huang
1,*,
Xinyue Chen
1,* and
Yujiang Xie
2
1
School of Earth Science and Spatial Information Engineering, Hunan University of Science and Technology, Xiangtan 411101, China
2
Jiangxi Fourth Geological Brigade, Pingxiang 337000, China
*
Authors to whom correspondence should be addressed.
Minerals 2023, 13(7), 943; https://doi.org/10.3390/min13070943
Submission received: 2 June 2023 / Revised: 11 July 2023 / Accepted: 12 July 2023 / Published: 14 July 2023
(This article belongs to the Section Mineral Deposits)
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Abstract

:
Mafic dikes are developed in the Shangsu region of Jiangxi, including Nanyuan Mountain and Mianhuaao. These dikes intrude into the Upper Triassic Anyuan Formation and are primarily composed of pyroxene, plagioclase, and opaque minerals, exhibiting a dolerite texture. The mafic dikes were found to have an SiO2 content ranging from 48.38% to 50.53% and the (K2O + Na2O) content ranging from 2.88% to 4.16%. The Na2O/K2O ratio was found to be between 2.56 and 3.99. The Eu anomaly was absent (δEu = 0.91–0.95), suggesting no influence of plagioclase fractionation during the rock formation process. The Ce anomaly was found to be absent (δCe = 1.04–1.08). The Mg# was found to range from approximately 40.06 to 45.06, indicating minimal crystal fractionation within the magma. The mafic dikes are enriched in light rare earth elements and large ion lithophile elements (LILE) and Th, while they showed significant depletion of high field strength elements (Nb, Ta, Ti). The Ti depletion may be related to the separation and crystallization of Ti-bearing minerals such as amphibole and ilmenite. Zr and Hf anomalies were evident, likely due to the contamination of zircon minerals in the samples. The mafic dikes were most likely products of the Middle–Late Yanshanian magmatic intrusion, formed in an extensional setting within the intracontinental rift environment caused by the collision of the Pacific Plate and the Eurasian Plate. The lithospheric mantle source was influenced by subduction zone fluid, and the magma source region exhibited mixed crustal materials.

1. Introduction

The South China region is a vital metal mineralization area in China, characterized by complex geological and tectonic evolution. It experienced a complex tectonic evolution since the early Cambrian and further underwent the assembly and breakup of global supercontinents and the amalgamation and separation of the North and South continents [1,2,3]. It is an essential component of global plate tectonic evolution [4,5,6,7].
This region is China’s largest granite uranium mineralization area, and previous researchers conducted extensive research work here [8,9]. Mesozoic mantle-derived magmatism’s spatial and temporal distribution in South China is closely related to uranium mineralization [10,11,12]. It was always a focus and challenge of research. mafic dikes are essential carriers of mantle information and are crucial in studying regional tectonic evolution [13,14,15,16]. Accurate isotopic dating and elemental geochemical studies can determine the temporal sequence of tectonic evolution and provide constraints for lithospheric evolution. These research results are of great significance for understanding regional geological evolution. The Shangsu area in Jiangxi is located in the western segment of the “Pingxiang-Shaoxing suture zone” within the “Qinhang eastern junction zone” where the Yangtze Plate and Huaxia Plate are combined, exhibiting a complex tectonic system. The area is situated at the junction of the Yangtze Block and the South China Fold Belt. The northern part corresponds to the western segment of the “Pingxiang-Le’an Depression”, the central part corresponds to the western segment of the “Wugongshan Uplift”, and the central-western and southern parts are part of the “Yongxin Depression”. The South China Block underwent the influence of three major tectonic systems, resulting in a superimposed and composite tectonic pattern. Due to its unique location and tectonic environment, it created favorable conditions for mineralization in the region, and previous researchers made some research achievements in this region [1,10,11,14,17,18,19,20,21,22,23,24,25,26,27,28,29,30,31,32,33,34].
Mafic dikes in the South China region received extensive research attention recently. By analyzing the formation environment of mafic dikes and their relationship with coeval granites, their impact on mineralization processes was investigated in depth [5,35,36,37]. In this study, samples of mafic dikes collected from Nanyuan Mountain in the Shangsu area were subjected to petrographic examination and major and trace element geochemical analysis. The aim was to investigate the origin, source characteristics, and geological significance of the mafic dikes in this region, providing valuable information for further analysis of the Mesozoic magmatic evolution and petrogenetic dynamics in the South China region.

2. Regional Geological Background

The Shangsu area in Jiangxi is located between the Yangtze Block and the Huaxia Block, with all exposure except the Upper Proterozoic, Lower Paleozoic, and Tertiary sediments. The traditional boundary between the Yangtze Platform and the South China Fold Belt is located south of this area, passing through the Pingle depression belt between the Jiuling and Wugong uplifts in central Jiangxi, trending northeast. The Shangsu area is located at the western end of the depression and is divided into two parts, north and south, which are connected east–west. The Middle Proterozoic Shuangqiao Formation and Devonian strata constitute an allochthonous system of thrusting and nappe structures along the southern margin of the Jiuling uplift, trending northeast. The Permian formations and Lower Triassic formations also have sporadic distributions. The Upper Triassic and Cretaceous are distributed in the central-western part of the study area, while the Quaternary is distributed in river systems and intermountain basins. The stratigraphy of the Shangsu area consists of the Neoproterozoic Shenshan Group and the Sinian metamorphic rocks, which are widely distributed. The overlying layers include the Cambrian, Devonian to Cretaceous, and Quaternary rocks. The geological evolution of the Shangsu area underwent a process of transition from oceanic to continental setting, which includes several stages. The first stage is the formation of the primitive continental crust from the Paleoproterozoic to the early Ediacaran, The second stage is the tectonic consolidation stage of the Cathaysia and Yangtze blocks during the South China Orogenic Movement, followed by the formation stage of the Wugongshan uplift from the late Ordovician to the early Silurian, the intracontinental Pingle depression stage from the late Paleozoic to the early Cretaceous, and the fault-controlled basin formation stage since the late Cretaceous. Ultimately, a three-layered structure of the uplifted basement, overlying cover basin, and fault-controlled basin was formed, with a structural pattern formed by the mutual superposition of the northeast and north-northeast-trending fault systems during the Yanshanian orogeny. The six samples of dolerite collected in this study intruded into the fine interbedded sandstone within deep gray, gray-black thin to medium-bedded mudstone and siltstone (Figure 1c).

3. Petrographic Characteristics of the Samples

The mafic dikes in Nanyuanshan have a width of about 100 m and extend for approximately 4500 m, with a strike direction of 320° and a dip angle of 42°. Another dike to the southwest has a width of about 70 m and extends for approximately 500 m, but its orientation is unclear. The two mafic dikes are controlled by northeast-southwest and east–west structural fractures. The samples were taken near the middle section of Nanyuan Mountain. The dolerite rocks were dark green in color, relatively complex, exhibiting intergrowth with elongated structures, diabasic textures, and blocky textures. The polarizing microscope used was the Leica DM2500P. Thin section identification under the microscope indicated that these samples mainly comprise clinopyroxene, plagioclase feldspar, and opaque minerals. JX001 and JX002 samples contained phenocrysts. The rocks were found to be composed of clinopyroxene (39%–45%), plagioclase feldspar (54%–60%), and opaque minerals (1%). The matrix plagioclase feldspar exhibited euhedral tabular morphology with a grain size of approximately 0.3–1 mm, and plagioclase is often affected by sericitization, the plagioclase laths are located chaotically and being internally filled with xenomorphic clinopyroxene. The diameter of the internally filled xenomorphic clinopyroxene is around 0.2–0.6 mm and the plagioclase laths are located chaotically. The phenocrystic clinopyroxene exhibited subhedral to xenomorphic columnar morphology with a grain size of 1.5–4 mm with prominent projections, and with interference colors reaching a third-order orange-red. It is commonly enclosed by euhedral tabular plagioclase feldspar with a grain size of approximately 0.3–0.6 mm. Opaque minerals were found to be present in small amounts, mainly iron-bearing minerals with varying grain sizes of 0.5–1 mm (Figure 2).

4. Analysis Methods and Results

A total of 6 sets of samples were tested, and fresh block-like rock samples were selected from the sampling area for analysis and testing conducted by Jiangxi Jinyuan Nonferrous Geological Testing Co., Ltd. The significant elements of the rocks were determined using an X-ray fluorescence spectrometer (model: Axios mAX (I-114)), while trace elements and rare earth elements were determined using an Inductively Coupled Plasma Mass Spectrometer (model: ICP-MS-7700x (I-100)). The analysis was conducted using national standards such as methods for chemical analysis of silicate rocks: GB/T14056.28-2010 and GB/T14506.30-2010, and the accuracy was better than 5%. The analytical results are shown in Table 1.

5. Geochemical Characteristics

The analyzed samples of Shangsu mafic dikes were found to have an SiO2 content ranging from 48.38% to 50.53%, which is normal. The MgO content ranged from 6.53% to 7.63%. The (K2O + Na2O) content ranged from 2.88% to 4.16%. The samples had a high Na2O content with Na2O > K2O; the range of Na2O/K2O was 2.56 to 3.99. In the SiO2-Nb/Yb diagram (Figure 3a), the rocks belonged to the sub-alkaline basalt region. Meanwhile, in the Th/Yb-Ta/Yb diagram (Figure 3b), it was classified under the calc-alkaline series. The range of Fe2O3 content was 8.96% to 9.59%. The Al2O3 content was relatively high, ranging from 16.63% to 17.81%. The range of CaO content was 6.41% to 9.01%. Additionally, the samples exhibited low TiO2 content ranging from 0.91% to 1.05%, with an average of 0.94%, indicating they belonged to the low-Ti basaltic rock series. The rare earth element abundance of the mafic dikes samples from the Shangsu area was (81.03~99.71) ppm, with an average of 87.43 ppm. The range of LREE/HREE ratio was 3.91 to 4.14, with an average of 4.02. The normalized distribution pattern of chondritic meteorites exhibited a differentiated with light rare earth element enrichment and heavy rare earth element depletion (Figure 4a). The range of (La/Yb)N was 3.20 to 3.57. The differentiation degree between LREE and HREE was not significant. The range of (La/Sm)N was 2.55 to 2.74, with an average of 2.67, while the range of (Gd/Lu)N was 0.98 to 1.05, with an average of 1.03. There was no significant differentiation between light and heavy rare earth elements. The samples showed no Eu anomaly (δEu = 0.91~0.96, with an average of 0.93), and Ce showed no anomaly (δCe = 1.02~1.06, with an average of 1.05). In the primitive mantle-normalized spider diagram (Figure 4b), the samples were significantly enriched in large ion lithophile elements (such as K, Rb, Ba, Th) and LREE, while high field strength elements Nb and Ti showed significant depletion. The shape of the trace element distribution curve exhibited a left-side peak and a gentle right-side slope. Zr and Hf showed positive anomalies. The range of the Rittmann index σ was 1.54 to 3.20, indicating that the samples belonged to the calc-alkaline rock series.

6. Discussion

6.1. Nature of Magma Source Region

The samples of dolerite from the Shangsu area exhibited a variation range of ignition loss from 2.87% to 4.42%, indicating a potential late-stage alteration influence. However, the high field strength elements (such as Zr, Nb, Pb, U) and immobile elements like rare earth elements and Ti were relatively less affected, making them better indicators of the characteristics of the magma source region and the genesis of the rocks. The dolerite dikes in the Shangsu are located in the sub-alkaline basalt field in the SiO2-Nb/Y diagram, and they are relatively enriched in large ion lithophile elements (K, Rb, Ba) and light rare earth elements. They were found to exhibit geochemical characteristics of depletion in high-field strength elements Nb, Ti, and P. The significant depletion of Nb indicates the characteristics of an island arc environment, while the depletion of Ti may be related to the separation and crystallization of Ti-bearing minerals such as ilmenite and titanomagnetite. The depletion of P suggests a low degree of apatite separation and crystallization. Th-U were higher than that of La. These facts along with negative anomalies of Nb and Ti were geochemical signatures of crustal contamination of mafic magmas. In the TiO2–Zr diagram (Figure 5a), the samples are located in the transitional zone between intra-plate basalts and volcanic arc basalts, suggesting possible influence from fluid-metasomatized mantle source region associated with subduction-induced dehydration [43]. The samples are located in the field of intra-plate basalt in the Zr/4-2Nb-Y diagram (Figure 5b). The samples are located in the continental margin arc region in the TH/Yb-Ta/Yb diagram (Figure 5c), indicating a possible enrichment of Th due to fluid-metasomatism in the mantle source region associated with subduction-induced dehydration [43], causing the sample to deviate from its original evolutionary trend. It projects onto the field of intra-plate basalt in the Zr/Y-Zr diagram (Figure 5d). In Figure 6a, all the samples belong to the crust-mantle source type, indicating that the magmatic formation process likely involved the participation of crustal material and fluids. The dolerite was rapidly intruded during the extensional tectonic stage of plate movement in southern China, suggesting a fast magma ascent. During this rapid ascent, the degree of crustal contamination will likely be minimal [18].
The samples in Figure 6b were located in the lithospheric mantle zone, and in Figure 7, the samples exhibited a trend of fluid-induced enrichment, indicating that the Shangsu dolerite was derived from a mantle source region enriched by subduction zone fluid. It suggests that the Shangsu dolerite is a product of fluid-rock interaction and melting in the lithospheric mantle, formed through the interaction between crustal material and dehydration of subducted slab. The enrichment in large ion lithophile elements (such as K, Rb, Ba) in the samples may be attributed to the fluids released during the phase transition of the subducted slab, carrying mobile elements such as K, Rb, Sr, and the interaction between the fluids and the overlying mantle wedge leading to the enrichment of these elements in the mantle wedge melting island arc magmas. Meanwhile, high-field strength elements do not enter the mantle wedge with water fluids, and the mantle wedge, enriched in significant ion lithophile elements, undergoes melting, resulting in high contents of LILE and relative depletion of HFSE.
The samples had relatively high Zr abundance of (159~1099) ppm, with JX-002 and JX-006 samples having Zr abundance of 1099 ppm and 1021 ppm, respectively, which was much higher than the other four samples. The high anomaly of Zr was speculated to be due to the assimilation of crustal zircon by mafic magma, with corresponding Hf abundance of 27.8 ppm and 26.3 ppm, also significantly higher than the other four samples. Together with Zr, Hf exhibited abnormally increased contents. The samples exhibited relatively high MgO contents (6.53%–7.63%), with an average value of 7.30%. The Mg# values ranged from 40.06 to 45.06, with an average of 43.43, lower than the original magma. The samples showed no Eu anomalies, the variation range of MgO content was 6.53%–7.63%, the variation range of SiO2 content was 48.38%–50.53%, and the variation range of Mg# content was 40.06%–45.06%, indicating magma differentiation and crystallization. The Na2O content in the samples was high, with Na2O > K2O. The Nb/U values ranged from 11.05 to 12.67, it was significantly lower than MORB and OIB and was located between the upper and lower crust, suggesting the presence of partial crustal material in the source region of the study area [47]. The Nb/Ta ratios ranged from 14.41 to 14.87, and the Zr/Hf ratios ranged from 36.15 to 39.55, generally consistent with the primitive mantle. The high ratios of La/Nb (>1.5) and La/Ta (>28) indicated characteristics of molten magma.
Minerals 13 00943 g006 550
Figure 6. (La/Yb)N–δEu (a) and La/Ba–La/Nb (b) diagrams of the Shangsu diabase. (a) adopted from [48], (b) adopted from [49].
Figure 6. (La/Yb)N–δEu (a) and La/Ba–La/Nb (b) diagrams of the Shangsu diabase. (a) adopted from [48], (b) adopted from [49].
Minerals 13 00943 g006
Minerals 13 00943 g007 550
Figure 7. Ba/La–Th/Yb (a) and Ba/Th–(La/Yb)N (b) diagrams of Shangsu diabase. Adopted from [48].
Figure 7. Ba/La–Th/Yb (a) and Ba/Th–(La/Yb)N (b) diagrams of Shangsu diabase. Adopted from [48].
Minerals 13 00943 g007

6.2. Tectonic Background

The Mesozoic magmatic activity in the South China region was widespread [14,23,50]. Researchers believe that during the Early Cretaceous, the tectonic pattern in South China transitioned from compression and uplift to extensional rifting. During this period, asthenospheric upwelling and lithospheric extension formed a series of mafic dikes, which exhibited characteristics of intra-plate basalt [35,43,51]. Most scholars believe that the multiple episodes of magmatic activity during the Jurassic to Cretaceous in an extensional setting were a response to the westward subduction of the Pacific Plate beneath the Eurasian continental plate [4,6,9,12,25,52]. According to the 1:50,000 geological map and explanatory notes of the study area, it is evident that the Late Triassic Anyuan Formation was intruded by dolerite dikes in the Shangsu region, which are products of the Late to Middle Yanshanian magmatic intrusion activity. This period coincided with the Pacific Plate’s reverse subduction and the continental lithosphere’s extensional thinning [9].
Additionally, according to research conducted by other scholars in the surrounding areas, the formation of basaltic dikes in Aikou, Dean County, occurred around 120 million years ago [18]. The U-Pb age of the Yingshan deposit in Dexing was determined to be 152 ± 10 million years [53]. The 39Ar-40Ar age of the Huangsha dolerite was determined to be 140 million years [54]. The U-Pb age of the Nancheng diabase in southern-central Jiangxi was determined to be 158.0 Ma ± 3.4 Ma [55]. Therefore, it can be inferred that the age of the Shangsu dolerite is around 150 million years, and it is a product of the Late to Middle Yanshanian magmatic intrusion activity. It formed in a tectonic setting characterized by an extensional environment due to the Pacific Plate subduction-induced lithospheric extension and thinning. The melting of the enriched mantle in the lithosphere occurred through fluid metasomatism resulting from the dehydration of the subducted slab.

7. Conclusions

(1) The Shangsu dolerite in the study area is a product of melting in the lithospheric mantle due to fluid metasomatism derived from the subducted slab, with evidence of crustal material mixing in the magma source.
(2) The mafic dikes distributed in the Shangsu area exhibited geochemical characteristics of intra-plate basalt. The lithospheric mantle source was influenced by subduction zone fluid. These mafic dikes are likely products of Late to Middle Yanshanian magmatic intrusion activity, formed in an intra-plate extensional environment resulting from the collision between the Pacific Plate and the Eurasian Plate.

Author Contributions

Fieldwork, Y.X. and X.C.; software, Y.H.; resources, X.C.; writing—review and editing, Y.H. All authors have read and agreed to the published version of the manuscript.

Funding

This research received no external funding.

Data Availability Statement

The data underlying this article are available in the article.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 13 00943 g001 550
Figure 1. Location (a,b) and geological sketch (c) of study area. (a) Adopted from [38], (b) adopted from [39], (c) adopted from the geological map from the Jiangxi Provincial Geological Information Center.
Figure 1. Location (a,b) and geological sketch (c) of study area. (a) Adopted from [38], (b) adopted from [39], (c) adopted from the geological map from the Jiangxi Provincial Geological Information Center.
Minerals 13 00943 g001
Minerals 13 00943 g002 550
Figure 2. Microscopic photographs and field photographs of the mafic dikes (a–d) is the number of Microscopic photographs; (e,f) is the number of field photographs; Px: pyroxene, PI: plagioclase, CPX: clinopyroxene, Por: Porphyritic.
Figure 2. Microscopic photographs and field photographs of the mafic dikes (a–d) is the number of Microscopic photographs; (e,f) is the number of field photographs; Px: pyroxene, PI: plagioclase, CPX: clinopyroxene, Por: Porphyritic.
Minerals 13 00943 g002
Minerals 13 00943 g003 550
Figure 3. SiO2—Nb/Y (a) and Th/Yb-Ta/Y (b) diagrams of the Shangsu dolerite (a) adopted from [40], (b) adopted from [41].
Figure 3. SiO2—Nb/Y (a) and Th/Yb-Ta/Y (b) diagrams of the Shangsu dolerite (a) adopted from [40], (b) adopted from [41].
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Minerals 13 00943 g004 550
Figure 4. Primitive mantle-normalized multi-element diagram (a) and reference values for primitive mantle and chondrite, (b) reference values for MORB and chondrite adopted from [42].
Figure 4. Primitive mantle-normalized multi-element diagram (a) and reference values for primitive mantle and chondrite, (b) reference values for MORB and chondrite adopted from [42].
Minerals 13 00943 g004
Minerals 13 00943 g005 550
Figure 5. Diagrams of discrimination for the tectonic setting of the Shangsu dolerite. (a) Adopted from [41], (b) adopted from [44], (c) adopted from [45], (d) adopted from [46].
Figure 5. Diagrams of discrimination for the tectonic setting of the Shangsu dolerite. (a) Adopted from [41], (b) adopted from [44], (c) adopted from [45], (d) adopted from [46].
Minerals 13 00943 g005
Table
Table 1. Major and trace element analyses of dolerite in the Shangsu area.
Table 1. Major and trace element analyses of dolerite in the Shangsu area.
Sample IDJX-001JX-002JX-003JX-004JX-005JX-006
LOI *4.174.424.113.492.873.63
SiO2 *50.5349.46 48.40 48.59 49.94 48.38
Al2O3 *16.6316.89 17.55 17.49 17.81 17.21
Fe2O3 *8.979.41 9.20 9.41 8.96 9.59
CaO *6.59 6.41 9.00 9.01 8.74 8.84
MgO *7.14 7.36 7.63 7.63 6.53 7.53
TiO2 *0.91 0.95 0.85 0.90 1.05 0.94
MnO *0.16 0.16 0.15 0.15 0.16 0.17
P2O5 *0.11 0.12 0.10 0.11 0.13 0.12
K2O *0.94 0.91 0.68 0.73 1.03 0.88
Na2O *3.68 3.64 2.20 2.30 2.63 2.48
V149 148 140 146 168 149
Cr217 300 263 260 215 219
Co37.0 38.7 40.2 40.7 34.0 38.2
Ni97.2 136 121 117 73.8 107
Ga15.8 15.3 15.7 16.5 16.5 15.4
Sr352 330 223 212 238 226
Zr248 1099 159 581 246 1021
Nb7.19 7.20 5.85 6.24 7.23 6.64
Ba382 349 166 163 253 204
Hf6.51 27.8 4.40 15.1 6.71 26.3
Ta0.49 0.48 0.41 0.43 0.50 0.46
Pb13.0 13.4 8.62 9.53 10.3 7.26
Th4.05 4.04 3.89 4.18 4.91 4.41
U0.58 0.57 0.51 0.56 0.65 0.60
Rb38.6 35.1 19.0 20.3 30.6 28.0
Sc26.9 30.6 23.9 25.1 30.7 27.4
Y31.8 89.0 27.8 56.2 37.7 86.0
La14.0 14.5 13.3 13.4 16.4 14.9
Ce30.1 32.0 29.5 30.5 36.4 33.4
Pr3.56 3.66 3.42 3.56 4.19 3.84
Nd14.4 15.2 14.1 14.9 17.4 15.8
Sm3.30 3.43 3.29 3.39 3.98 3.53
Eu1.07 1.10 1.10 1.11 1.27 1.13
Gd3.66 3.98 3.72 3.92 4.57 4.09
Tb0.66 0.69 0.65 0.67 0.80 0.71
Dy4.18 4.41 4.33 4.51 5.24 4.81
Ho0.95 0.99 0.95 1.01 1.17 1.06
Er2.86 3.08 2.86 3.05 3.60 3.16
Tm0.45 0.44 0.44 0.46 0.53 0.48
Yb2.81 3.05 2.94 3.00 3.53 3.21
Lu0.46 0.48 0.45 0.46 0.54 0.48
LREE/HREE4.144.083.963.913.994.03
Mg#43.2843.3443.9144.9140.0645.06
δEu0.940.910.950.930.910.909
δCe1.041.071.071.081.071.08
LaN/YbN3.573.413.253.203.333.33
Note: Major element concentrations have been recalculated on a dry basis. Element concentrations marked with * are given in percentage (%), while other units are in parts per million (ppm).
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Huang, Y.; Chen, X.; Xie, Y. Geochemical Characteristics and Geological Significance of the Shangsu Mafic Dikes in Jiangxi. Minerals 2023, 13, 943. https://doi.org/10.3390/min13070943

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Huang Y, Chen X, Xie Y. Geochemical Characteristics and Geological Significance of the Shangsu Mafic Dikes in Jiangxi. Minerals. 2023; 13(7):943. https://doi.org/10.3390/min13070943

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Huang, Yang, Xinyue Chen, and Yujiang Xie. 2023. "Geochemical Characteristics and Geological Significance of the Shangsu Mafic Dikes in Jiangxi" Minerals 13, no. 7: 943. https://doi.org/10.3390/min13070943

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