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Article

Ancient Metasomatism in the Lithospheric Mantle, Eastern North China Craton: Insights from In-Situ Major and Trace Elements in Garnet Xenocrysts, Mengyin District

by
Hao-Shuai Wang
1,2,
Li-Qiang Yang
1,2,*,
Zhi-Yuan Chu
3,4,
Liang Zhang
1,5,*,
Nan Li
1,
Wen-Yan He
1,
Ya-Nan Zhang
2 and
Yi-Qi Wang
5
1
State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Beijing 100083, China
2
School of Earth Sciences and Resources, China University of Geosciences, Beijing 100083, China
3
The 7th Institute of Geology & Mineral Exploration of Shandong Province, Linyi 276006, China
4
Key Laboratory of Diamond Mineralization Mechanism and Exploration, Shandong Provincial Bureau of Geology & Mineral Resources, Linyi 276006, China
5
School of Gemmology, China University of Geosciences, Beijing 100083, China
*
Authors to whom correspondence should be addressed.
Minerals 2023, 13(8), 1106; https://doi.org/10.3390/min13081106
Submission received: 8 July 2023 / Revised: 14 August 2023 / Accepted: 18 August 2023 / Published: 20 August 2023
(This article belongs to the Section Mineral Deposits)
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Abstract

:
Mantle metasomatism refers to the interaction between mantle melt, fluid, and mantle rock. It not only affects the physical and chemical properties of the lithospheric mantle but also plays an important role in the process of metal and gem mineralization. In order to explore the nature and evolution of metasomatism in the lithospheric mantle of the Mengyin area in the eastern part of the North China Craton, this paper combines the previous data of garnet inclusions in diamonds and analyzes the major and trace elements of garnet xenocrysts in the Shengli No. 1 kimberlite pipe from the EPMA and LA-ICP-MS experiments. The experiments show that the garnet xenocrysts of the Shengli No. 1 kimberlite pipe are mainly lherzolitic and harzburgitic garnets. The content of Zr and TiO2 in some garnets are low, which are the characteristics of depleted garnets. Conversely, another group of garnets display high Zr and TiO2 contents, indicative of high-temperature melt metasomatism. When comparing the Ti/Eu ratio of the depleted garnets to that of the primary mantle, a significantly lower value is observed. Additionally, the (Sm/Er)N value undergoes minimal changes, while the Zr/Hf value exceeds that of the primary mantle. These characteristics are indicators of carbonatite melt metasomatism. Garnets that are affected by high-temperature melt metasomatism exhibit low (Sm/Er)N content, a significant variation in the Ti/Eu ratio, and a Zr/Hf value greater than that of the primary mantle. These characteristics indicate the influence of kimberlite melt metasomatism. Garnets impacted by carbonatite melt metasomatism display a strong sinusoidal distribution pattern of rare earth elements (REE) and are often found as lherzolitic garnet xenocrysts and garnet inclusions in diamond. On the other hand, garnets influenced by kimberlite melt metasomatism exhibit a slight sinusoidal REE distribution pattern in harzburgitic garnets and a slight sinusoidal REE distribution or a flat pattern from medium rare earth elements (MREEs) to heavy rare earth elements (HREEs) in lherzolitic garnet xenocrysts. Based on these findings, it is evident that there are at least two types of metasomatism occurring in the lithospheric mantle of the Mengyin area in the eastern part of the North China Craton. The first type involves the metasomatism of early carbonatite melt to the mantle peridotite. Garnets formed under this condition exhibit high Sr and LREE contents, as well as low Zr, Hf, Ti, Y, and HREE contents, indicating depletion characteristics. The second type entails the metasomatism of late kimberlite melts affecting the mantle peridotite. Garnets formed under this process display high Zr, Hf, Ti, Y, and HREE contents.

1. Introduction

Kimberlites found in ancient stable cratons bring mantle xenoliths from depleted and low-density areas in the mantle to the earth’s surface, providing a rare window for the study of the lithospheric mantle (SCLM) [1]. Mantle metasomatism has been observed in mantle xenoliths worldwide and has significant implications for the physical and chemical characteristics of the lithospheric mantle, as well as the processes of deep metallogenic and crust-mantle evolution [2,3,4,5,6,7,8,9,10,11,12,13]. Highly depleted mantle harzburgites are remnants of the partial melting of the primitive mantle and subsequently metasomatized by mantle melts [14]. Metasomatic melts and fluids play a crucial role in chemical exchanges within the mantle, redistributing elements from previously depleted regions of the mantle [15,16,17,18,19,20]. There are various types of metasomatism in the lithospheric mantle, including (1) low-temperature (950–1100 °C) metasomatism associated with phlogopite crystallization [16,17,18,19,20,21]; (2) carbonatite melt metasomatism [16,17,18,19,20,21,22]; (3) kimberlite melt metasomatism [1,23]; and (4) metasomatism of basaltic magma [1,5]. The major minerals of the peridotite in the lithospheric mantle are olivine, garnet, orthopyroxene, and clinopyroxene. The characteristics of their major and trace elements reflect the melting and metasomatism processes of their host rocks and record essential information on the evolution of the lithospheric mantle of the Archean craton [1,5,7,16,23,24,25].
Garnet is known to be more resistant to preservation compared to olivine and pyroxene during the processes of kimberlite magmatism and surface weathering. Harzburgitic garnet inclusions in diamonds are relatively common and exhibit characteristics such as high Cr content and low Ca content. These features make harzburgitic garnets indicative for diamond prospecting [26,27,28,29,30,31]. The nature and timing of garnet formation are of great significance for understanding the evolution of the lithospheric mantle. For instance, the garnet core of the Wesselton kimberlite in South Africa has low Ca, Y, Ga, and Zr contents and a sinusoidal rare earth elements (REE) distribution pattern, indicating that the garnet core is related to the carbonatite melt metasomatism. The gradual increase in Ca, Y, Ga, and Zr from the core to the rim indicates a progressive enrichment in the garnet composition due to mantle metasomatism [21]. In Siberian mantle xenoliths, two distinct trends of garnet composition are observed. In the harzburgite region, there is little variation in Cr2O3 content, while CaO content gradually increases. In the lherzolite region, both CaO and Cr2O3 decrease gradually. These trends indicate that garnet evolves from an ultramafic composition towards a mafic composition under the influence of mantle metasomatism. The garnet grains exhibit a sinusoidal REE distribution pattern in the core and a flat pattern from medium rare earth elements (MREEs) to heavy rare earth elements (HREEs) with high Ti/Eu ratios at the edge, indicating the influence of kimberlite melt metasomatism [1,23].
The eastern North China Craton is known for its significant deposits of gold, rare earth ores, and diamonds. Recent studies have revealed that metasomatic processes in the lithospheric mantle play a crucial role in the formation of ore deposits in this region [32,33,34,35,36,37,38]. However, the unclear process and mechanism of mantle metasomatism restrict the understanding of the formation process and deep drive of deposits in this area. A large number of diamondiferous kimberlites are exposed in the Mengyin area, where garnet xenocrysts are developed and a large amount of mantle-derived metasomatism information is recorded. It is an ideal choice to explore the mantle metasomatism in the eastern North China Craton. Indeed, extensive research has been conducted on the geochemical characteristics of garnet in kimberlite and the mineralogical characteristics of diamonds in the Mengyin area of the eastern North China Craton. Pyroxene-garnet thermobarometry was used to measure the temperature and pressure of diamond formations. The formation temperature of diamonds in Mengyin is between 1100 °C and 1203 °C, along with pressures ranging from 5.59 GPa to 9.20 GPa [39]. Garnets in peridotite xenoliths and garnet megacrysts in Mengyin have undergone a complete transformation due to metasomatic fluid. This transformation indicates an enrichment of the mantle [40]. The harzburgitic garnet inclusions in diamond have high light rare earth element (LREE) content and relatively low high field strength element (HFSE) content, which aligns with the metasomatism caused by carbonatite melts [14]. Additionally, the garnet cell parameter in Mengyin’s kimberlites exhibits a significant decreasing trend from lean ore-bearing rocks to rich ore-bearing rocks [41]. The presence of harzburgitic garnet has indicative significance for diamond prospecting, based on a study of the major elements CaO and Cr2O3 in garnet [42]. Through the analysis of inclusion minerals in diamonds, it has been estimated that the depth of the kimberlite magma source and the lithosphere thickness in the eastern part of the Paleozoic North China Craton are about 200 km [43]. An analysis of carbon isotope composition indicated that the carbon forming diamonds in Mengyin originated from the deep mantle, suggesting that the lithospheric mantle had not been modified by the subducted oceanic crust before the eruption of the kimberlite [44].
Significant progress has been made in understanding the characteristics of kimberlites, the lithospheric mantle structure, and crust-mantle evolution in the area. However, the genesis of garnet xenocrysts in Mengyin kimberlites, the geochemical characteristics of metasomatic melts/fluid, and the sequencing of metasomatism still require further investigation due to the complex nature of deep geological processes in the mantle.
Therefore, this paper intends to determine the type and sequence of lithospheric mantle metasomatism in the Mengyin area by analyzing the major and trace elements of eight garnet xenocrysts from the Shengli No. 1 kimberlite pipe in Mengyin and to find out the geochemical characteristics of metasomatic melts. The evolution process of mantle metasomatism provides a reference for understanding the nature and evolution of lithospheric mantle metasomatism and the formation and preservation environment of diamond in the Mengyin area.

2. Geological Background

The Mengyin kimberlite is located in the central part of the Luxi block within the eastern part of the North China Craton. It is 60~70 km east of the Tanlu fault zone (Figure 1).
The NW-trending faults include the Caizhuang fault, Duozhuang fault, and Mengshan fault. They are the main faults in this area. These faults have a significant length of over 100 km, striking in the range of 310° to 340°, and dipping at angles between 55° and 85°. Some small-scale NW-trending faults are more developed, among which the NWW-trending tensional faults have a certain control effect on the formation of kimberlite pipes. The NE-trending Shangwujing fault, which has a length of about 250 km, is also the main fault in the region. Additionally, the NNE-trending faults are well developed, and it is in these faults that some kimberlite veins are predominantly filled [47,48]. The wall rock of the kimberlite is mainly Archean Taishan Group mixed gneiss, and a few lean ore-bearing rock masses are produced in Cambrian–Ordovician limestone and shale. Additionally, the area is known for its exposures of granite, diorite porphyrite, diabase, and carbonate rocks [39,47,48,49,50].
The Mengyin kimberlite region is characterized by three main rock belts: the Changmazhuang rock belt, the Xiyu rock belt, and the Poli rock belt. These rock belts are arranged from south to north, with a gradual weakening of their ore-bearing properties. The Changmazhuang rock belt is located near Changmazhuang in the southwest of the Mengyin kimberlite area, approximately 13 km away from the Mengyin county. It consists of eight dykes and two rock pipes. The overall trend of the rock belt is NW at 345°, with a length of about 14 km and a width of 2.5 km. The dykes are arranged in a right column. Their trend ranges from 15° to 35°, forming an angle of 30° to 50° with the overall trend of the rock belt [47,48]. The Shengli No. 1 kimberlite pipe in the Changmazhuang rock belt is the highest ore-bearing deposit in the Mengyin area, and the diamond grade is generally 100–800 mg/m3. The lithology of the Shengli No. 1 kimberlite pipe is mainly porphyritic kimberlite, with a relatively high content of pyrope [48,49,51].

3. Samples and Analytical Techniques

3.1. Petrography

The kimberlite is dark green as a whole, and the serpentinization is strong. Most of the olivine has been altered into serpentine, but the illusion of olivine is still preserved (Figure 2a,b). Garnet is elliptical as a whole, and the edge alteration is reddish-brown kelyphite (Figure 2c–f). From the backscattered images, it can be seen that some garnets have a high degree of fragmentation and a strong alteration, and the edges and fissures in the garnet grains are filled with iron oxides (Table 1; Figure 2e,f). No banding phenomenon was found in the garnet xenocryst samples (Figure 2g,h).

3.2. Analytical Techniques

The major element analysis of garnets was conducted using an electron microprobe analyzer (EPMA; JXA-8100, JEOL of Japan) at the Institute of Geology, Chinese Academy of Geological Science. The analysis was carried out with a 15 kV accelerating voltage, 20 nA probe current, and 5 μm beam diameter. Fifty-three kinds of natural and synthetic minerals from the SPI Company were used for standardization, and ZAF corrections were carried out.
The trace element analysis of garnets was performed using LA-ICP-MS at the State Key Laboratory of Mineral Deposit Geochemistry, Institute of Geochemistry, Chinese Academy of Sciences. The instruments used were the RESOlution-SE laser ablation system and Agilent 7900 inductively coupled plasma mass spectrometry (ICP-MS). During the analyses, a laser repetition rate of 5 to 6 Hz and an energy density of 4 to 5 J/cm2 were used. The laser spot sizes are 50 μm. SRM610 was used to optimize the performance of ICP-MS before the test so that the instrument achieved the best sensitivity and ionization efficiency (U/Th ≈ 1), the smallest possible oxide yield (ThO/Th < 0.3%), and a low background value. The standard samples are USGS glasses (BCR-2G, BIR-1G and BHVO-2G). TB-1G and NKT-1G without correction were used as quality control samples. The recommended values of element content in these silicate glasses are based on the GeoReM database (http://georem.mpch-mainz.gwdg.de/, accessed on 1 April 2023).

4. Results

4.1. Major Elements

The major element data of garnet xenocrysts in the Shengli No. 1 kimberlite pipe are shown in Table 2. All the major element data of garnets are shown in Table S1 of the Supplementary Materials. The end-member calculation of the garnets is shown in Table S2 of the Supplementary Materials, and the structural formula calculation of garnets is shown in Table S3 of the Supplementary Materials. The relationship between CaO and Cr2O3 is usually used to classify garnet xenocrysts [26]. Based on this classification, the majority of garnet xenocrysts from the Shengli No. 1 kimberlite pipe fall within the lherzolite area, while only the sample SL5-1 falls into the harzburgite area (Figure 3a). Harzburgitic garnet xenocrysts have a lower Ca content (CaO 4.76–5.11 wt.%), higher Cr content (Cr2O3 7.13–7.51 wt.%), and higher Ti content (TiO2 0.35–0.88 wt.%). On the other hand, lherzolitic garnet xenocrysts have a higher Ca content (CaO 4.68–5.78 wt.%), lower Cr content (Cr2O3 4.12–7.64 wt.%), and a larger variation range of Ti content (TiO2 0–1.14 wt.%) (Figure 3b).

4.2. Trace Elements

The trace element data of garnet xenocrysts in the Mengyin Shengli No. 1 kimberlite pipe are shown in Table 3. All the trace elements of garnets are shown in Table S4 of the Supplementary Materials. The REE distribution patterns of garnet xenocrysts were divided into two types: (1) the sinusoidal REE group, (Sm/Er)N > 1 and (Tm/Yb)N < 1; and (2) the flat MREE–HREE group, (Sm/Er)N < 1 and (Tm/Yb)N ≤ 1 [1]. Only the MREE–HREE distribution curve of SL1-2 is flat (Figure 4f and Figure 5a,b).
The harzburgitic garnet xenocrysts exhibit a sinusoidal pattern in their REE distribution, as shown in Figure 4d. From La to Sm, the LREE content gradually increases. From Sm to Er, the MREE content decreases gradually. From Er to Lu, HREE increases slowly. The (Sm/Er)N value for these garnet xenocrysts ranges from 2.44 to 4.47, indicating a moderate enrichment in MREEs relative to HREEs. The (Tm/Yb)N value ranges from 0.68 to 1.44, suggesting a slight depletion in HREEs compared to MREEs. In terms of trace element composition, the Sr content ranges from 0.98 to 1.52 ppm, the Y content ranges from 5.16 to 5.92 ppm, the Zr content ranges from 25.86 to 46.97 ppm, the Hf content ranges from 0.56 to 0.85 ppm, and the Ni content ranges from 113.69 to 120.77 ppm.
Based on the shape of chondrite-normalized rare earth element (REE) patterns, lherzolitic garnets in the Shengli No. 1 kimberlite pipe can be classified into three groups: those with a strongly sinusoidal REE pattern (Lz1, Figure 4c), those with a slightly sinusoidal REE pattern (Lz2, Figure 4d,e), and those with a flat MREE–HREE pattern (Lz3, Figure 4f).
The Lz1 group garnets (SL5-2, SLJ5-2) exhibit a strongly sinusoidal REE pattern. They have a Cr2O3 content ranging from 4.95 to 5.72 wt.%, CaO content ranging from 5.05 to 5.47 wt.%, TiO2 content ranging from 0 to 0.6 wt.%, Sr content ranging from 0.60 to 0.89 ppm, Y content ranging from 1.29 to 1.97 ppm, Zr content ranging from 1.05 to 30.65 ppm, Hf content ranging from 0 to 0.55 ppm, and Ni content ranging from 59.33 to 97.62 ppm. The Lz2 group garnets (SL1-1, SL7-1, SL11-1) show a slightly sinusoidal REE pattern. They have a Cr2O3 content ranging from 4.14 to 7.64 wt.%, CaO content ranging from 4.76 to 5.78 wt.%, TiO2 content ranging from 0.17 to 1.14 wt.%, Sr content ranging from 0.34 to 19.01 ppm, Y content ranging from 3.51 to 8.50 ppm, Zr content ranging from 9.84 to 112.12 ppm, Hf content ranging from 0.17 to 2.93 ppm, and Ni content ranging from 52.95 to 1015.15 ppm. The Lz3 group garnets (SL1-2) display a flat MREE–HREE pattern. They have a Cr2O3 content ranging from 5.05 to 5.41 wt.%, CaO content ranging from 4.73 to 4.95 wt.%, TiO2 content ranging from 0.39 to 0.52 wt.%, Sr content ranging from 0.45 to 1.65 ppm, Y content ranging from 12.01 to 12.71 ppm, and Zr content ranging from 31.49 to 32.62 ppm.
The garnet inclusions found in diamonds from the Shengli No. 1 kimberlite pipe, as reported by [14], are characterized by high contents of Cr2O3, Sr, and LREE. These inclusions exhibit low contents of CaO, TiO2, Y, Zr, and HREE. Their REE distribution pattern is sinusoidal.

5. Discussion

5.1. The Genesis of Peridotitic Garnet

The depleted peridotite of lithospheric mantle is generally considered to be remnant of the high-degree partial melting of early enriched peridotites [53,54,55,56]. During the process of partial melting, incompatible elements such as Zr, Ti, Hf, Y, and Sr enter the melt, leading to low contents of these elements in the mantle rocks. Although some garnets can survive partial melting [15], clinopyroxenes and garnets in depleted peridotites may still undergo metasomatism [5,57].
The depleted garnets represent the residual phase of the partial melting in the mantle and inherits the characteristics of low CaO and trace element contents from the host rock. It exhibits a positive-slope rare earth element pattern after chondrite standardization [40]. In the Shengli No. 1 kimberlite pipe, the depleted garnet xenocrysts demonstrate low Ca and high Cr contents, along with low concentrations of trace elements such as Zr, Ti, Hf, and Y. They exhibit a sinusoidal rare earth element pattern (Figure 4c,d), which is consistent with the features of rare earth element enrichment through metasomatism [58]. Hence, the garnet xenocrysts in the Shengli No. 1 kimberlite pipe cannot be solely explained as the residues of partial melting but are also associated with mantle metasomatism processes.
The Zr-TiO2 diagram is commonly used to distinguish between depleted garnets and metasomatic garnets [21]. Metasomatism can be classified into two types: low-temperature metasomatism (occurring at temperatures of 950–1100 °C), associated with phlogopite crystallization, and high-temperature metasomatism [1,21,23]. The metasomatism resulting from kimberlite melts and basalt melts (silicate melts) falls under high-temperature metasomatism [23]. In the early stages of low-temperature metasomatism, Zr gradually increases, Y slightly increases, and Ti shows a slow growth. Subsequently, Ca, Zr, Y, and Ti experience a sharp increase. In the Zr-TiO2 diagram (Figure 6), garnet xenocrysts belonging to the Lz2 group (SL1-1, SL7-1, SL11-1) and Lz3 group (SL1-2) are located in the high-temperature metasomatism region. On the other hand, the Lz1 group (SL5-2, SLJ5-2) and garnet inclusions in diamonds are situated in the depleted region.
The relationships between (Sm/Er)N and Ti/Eu in garnet can indicate different types of metasomatism (Figure 7a). It can be seen from Figure 7a that Lz1 garnets and garnet inclusions in diamonds from the Shengli No. 1 kimberlite pipe show a weak trend of carbonatite melt metasomatism. To further distinguish between metasomatism by carbonatite melts and kimberlite melts, Zr/Hf and Ti/Eu diagrams are used [16,22,25,59]. As depicted in Figure 7b, the Lz1 garnets are positioned within the region of carbonatite melt metasomatism, and the garnet inclusions in diamonds are close to this area, consistent with the findings in Figure 7a. The HREE, Y, Zr, and Hf contents of garnets are little affected by the metasomatism of carbonatitic melts, so it is reasonable that these garnets metasomatized by carbonatitic melts are located in the depleted region in the Zr-TiO2 diagram [16].
In Figure 7a, the Hz (SL5-1) and Lz2 (SL1-1, SL7-1, SL11-1) groups display a trend associated with silicate metasomatism. Combining this with Figure 7b, it is speculated that Hz and Lz2 (SL1-1) have undergone superimposed metasomatism by both carbonatite melts and kimberlite melts. The Ti/Eu ratio in Lz2 (SL7-1, SL11-1) is higher than that of the primitive mantle but exhibits a higher Zr/Hf value compared to chondrites (Figure 7b). The elevated TiO2 content may be attributed to Fe-Ti metasomatism in the residually high Cr and low Ca mantle [16]. Lz2 (SL7-1, SL11-1) displays metasomatism related to silicate melts in Figure 7a and is close to the metasomatism associated with kimberlite melts in Figure 7b. This suggests that Lz2 (SL7-1, SL11-1) and Lz3 may have undergone metasomatism by kimberlite melts.
On the whole, the garnet inclusions in diamonds and Lz1 (SL5-2, SLJ5-2) garnet xenocrysts record slight metasomatism of carbonatite melts. The garnet xenocrysts of Lz2 (SL1-1, SL7-1, and SL11-1) and Lz3 (SL1-2) record kimberlite melt metasomatism.

5.2. The Process of Metasomatism in the Mantle

Mantle metasomatism is a commonly observed process that alters peridotite rocks. It involves an enrichment in the mineral and chemical composition within the original mantle material through interactions with active melts and fluids, leading to spatially variable chemical compositions within the mantle [1,2]. This metasomatism, driven by the infiltration of fluids or melts, can result in changes in the concentrations of Ca, Fe, Ti, Y, Zr, and rare earth elements (REE) in the lithospheric mantle [8].
Carbonatite melts have begun to transform the mantle since the Archean [60,61]. Kimberlite melts, which are CO2- rich magmas, are closely associated with carbonatite melt. The related carbonatite melts can be traced back to at least about 2.8 Ga ago, and some diamonds even recorded the event 3.3 Ga ago [62]. This also indicates that the metasomatism of carbonatite melts in the mantle can be traced back to at least 2.8 Ga ago. In this paper, it is found that both garnet inclusions in diamond and Lz1 garnet are metasomatized by carbonatite melts, indicating that the metasomatism of carbonatite melts occurred long before the formation of diamond.
Kimberlite magma is usually derived from the partial melting of carbonatized mantle peridotite [63,64]. Based on Sr-Nd-Hf isotope studies, the formation of kimberlites is related to the subduction of the ancient oceanic lithosphere into the interior of the North China Craton [64]. The different Hf isotopic compositions of Mengyin and Wafangdian kimberlites may reflect the different proportions of subducted oceanic crust, lithosphere, and asthenosphere during the formation of kimberlites. The formation of kimberlite magma requires small perturbations in the normal thermal structure of the deeper mantle [39]. Paleozoic mantle plume may exist in the North China Craton [23,65]. These mantle plumes may also trigger kimberlite magmatism in the North China Craton [66].
The harzburgitic garnet xenocrysts in the No. 30 kimberlite pipe of Wafangdian, Liaoning Province, show a strong sinusoidal REE distribution pattern, with low Y, Zr, and Ti contents [23]. These depleted garnets indicate metasomatism by carbonatite melts. In contrast, the harzburgitic garnet xenocrysts from the Shengli No. 1 kimberlite pipe display a slightly sinusoidal REE distribution pattern, with higher content of HREE compared to the harzburgitic garnets from the Wafangdian No. 30 kimberlite pipe. The HREE content of Lz3 garnet xenocrysts in the Shengli No. 1 kimberlite pipe is higher than that of the Lz3 garnet xenocrysts in the Wafangdian No. 30 kimberlite pipe [23]. This shows that the kimberlite melt metasomatism recorded in Mengyin is stronger than that in the Wafangdian area.
Based on the analysis of garnet xenocrysts in the Shengli No. 1 kimberlite pipe and the study of garnet inclusions in diamonds, a model of mantle metasomatism can be established, which involves two distinct stages: early carbonatite melt metasomatism and late kimberlite melt metasomatism.
During the first stage, the lithospheric mantle undergoes metasomatism by early LREE-rich carbonatite melts. This process leads to the formation of garnet inclusions in diamonds and Lz1 garnet xenocrysts. The age of the diamonds is significantly older than that of kimberlites, with the emplacement age of the Mengyin kimberlite estimated at around 465 million years ago [64,66]. Therefore, this stage predates 465 Ma. During this metasomatism, the concentrations of LREE gradually increase in garnet [1,23], as shown in Figure 4a (trend 1).
In the second stage, the partial melting of carbonatized peridotite in the lithospheric mantle generates kimberlite melts. The kimberlite magma subsequently metasomatizes the mantle peridotite. At this stage, the Lz1 garnet xenocrysts, characterized by a strong sinusoidal REE distribution pattern, transform into Hz and Lz2 garnet xenocrysts with a slightly sinusoidal REE distribution. Prior to the eruption of the host kimberlite, Lz2 garnets further transformed into Lz3 garnet xenocrysts with a flat MREE–HREE distribution following multiple metasomatism events by kimberlite melt [23]. Kimberlite melt metasomatism is responsible for the reduction in Cr2O3 content and the gradual increases in the concentrations of Y, Zr, Ti, and HREE in lherzolitic garnets (Figure 4a trend 2).

6. Conclusions

The analysis of garnet xenocrysts from the Mengyin Shengli No. 1 kimberlite pipe reveals that the mantle-derived garnets in this area are predominantly lherzolitic and harzburgitic garnets, which are closely related to mantle metasomatism. The depleted garnets, characterized by low contents of Zr, TiO2, and Y, exhibit a Ti/Eu ratio lower than that of the primary mantle and show little variation in (Sm/Er)N values, indicating the typical features of carbonatite melt metasomatism. On the other hand, garnets with high concentrations of Y, Zr, and TiO2, and low (Sm/Er)N values, along with a wide range of Ti/Eu ratios and Zr/Hf ratios greater than that of the primary mantle, exhibit characteristics of kimberlite melt metasomatism. The garnet inclusions in diamonds and Lz1 garnet xenocrysts mainly record early carbonatite melt metasomatism. These garnets display high Cr and Sr contents, low Y, Zr, Ti, and HREE contents, and exhibit a sinusoidal distribution of REE. In contrast, the Lz2, Lz3, and harzburgitic garnet xenocrysts record late-stage kimberlite melt metasomatism. These garnets demonstrate increasing concentrations of Y, Zr, Ti, and HREE, display a slightly sinusoidal REE distribution, and develop a flat MREE–HREE distribution.

Supplementary Materials

The following supporting information can be downloaded at: https://kdocs.cn/l/cdHQmIdnu1hC, accessed on 14 August 2023, Table S1: all the major elements data of garnets. Table S2: the end-member calculation of garnets. Table S3: the structural formula calculation of garnets. Table S4: all the trace elements of garnets.

Author Contributions

Conceptualization, H.-S.W.; methodology, L.-Q.Y., L.Z. and W.-Y.H.; software, H.-S.W., Y.-N.Z. and Z.-Y.C.; validation, H.-S.W. and L.Z.; formal analysis, H.-S.W., L.Z., L.-Q.Y. and W.-Y.H.; investigation, H.-S.W., Z.-Y.C. and N.L.; resources, H.-S.W., Z.-Y.C. and N.L.; data curation, H.-S.W.; writing—original draft preparation, H.-S.W.; writing—review and editing, H.-S.W., L.Z., L.-Q.Y.; visualization, H.-S.W. and Y.-Q.W.; supervision, H.-S.W., L.-Q.Y. and L.Z.; project administration, L.Z.; funding acquisition, L.-Q.Y. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the National Key Research Program of China (Grant No. 2019YFA0708603), the 111 Project of the Ministry of Science and Technology, China (Grant No. BP0719021), the open project of Observation and Research Station of Primary Diamond Deposits in Mengyin Shandong, Ministry of Natural Resources and Key Laboratory of Diamond Mineralization Mechanism and Exploration, Shandong Provincial Bureau of Geology & Mineral Resources (Grant No. QDKF-ZD202304) and MOST Special Fund from the State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences (Grant No. MSFGPMR201804).

Data Availability Statement

Not applicable.

Acknowledgments

Jun Deng, Kun-Feng Qiu, and Xue Gao from China University of Geosciences (Beijing) provided valuable support and guidance throughout the research process. Additionally, the experimental work conducted in this study received support and assistance from Xiao-Hong Mao, Qing-Lin Li from the Electron Probe Laboratory, Institute of Geology, Chinese Academy of Geological Sciences, and De-Feng He from the State Key Laboratory of Deposit Geochemistry, Institute of Geochemistry, Chinese Academy of Sciences. Furthermore, the participation of Xiao-Meng Ye, Dong Xie, Guan-Wen Shen, Wei Yang, Rui-Rui Zhang, Song Zhang, Ming-Li Li, and others in various aspects of the work is also acknowledged and appreciated. Thanks to everyone involved.

Conflicts of Interest

The authors declare no conflict of interest.

References

  1. Howarth, G.H.; Barry, P.H.; Pernet-Fisher, J.F.; Baziotis, I.P.; Pokhilenko, N.P.; Pokhilenko, L.N.; Bodnar, R.J.; Taylor, L.A.; Agashev, A.M. Superplume Metasomatism: Evidence from Siberian Mantle Xenoliths. Lithos 2014, 184–187, 209–224. [Google Scholar] [CrossRef]
  2. Menzies, M.A.; Rogers, N.; Tindle, A.; Hawkesworth, C.J. Metasomatic and Enrichment Processes in Lithospheric Peridotites, an Effect of Asthenosphere-Lithosphere Interaction. Mantle Metasomat. 1987, 119, 313–361. [Google Scholar]
  3. Ionov, D.A.; Dupuy, C.; O’Reilly, S.Y.; Kopylova, M.G.; Genshaft, Y.S. Carbonated Peridotite Xenoliths from Spitsbergen: Implications for Trace Element Signature of Mantle Carbonate Metasomatism. Earth Planet. Sci. Lett. 1993, 119, 283–297. [Google Scholar] [CrossRef]
  4. Coltorti, M.; Bonadiman, C.; Hinton, R.W.; Siena, F.; Upton, B.G.J. Carbonatite Metasomatism of the Oceanic Upper Mantle: Evidence from Clinopyroxenes and Glasses in Ultramafic Xenoliths of Grande Comore, Indian Ocean. J. Petrol. 1999, 40, 133–165. [Google Scholar] [CrossRef]
  5. Agashev, A.M.; Ionov, D.A.; Pokhilenko, N.P.; Golovin, A.V.; Cherepanova, Y.; Sharygin, I.S. Metasomatism in Lithospheric Mantle Roots: Constraints from Whole-Rock and Mineral Chemical Composition of Deformed Peridotite Xenoliths from Kimberlite Pipe Udachnaya. Lithos 2013, 160–161, 201–215. [Google Scholar] [CrossRef]
  6. Shchukina, E.; Agashev, M.A.; Pokhilenko, N.P. Metasomatic origin of garnet xenocrysts from the V.Grib kimberlite pipe, Arkhangelsk region, NW Russia. Geosci. Front. 2017, 8, 641–651. [Google Scholar] [CrossRef]
  7. Jollands, M.C.; Hanger, B.J.; Yaxley, G.M.; Hermann, J.; Kilburn, M.R. Timescales between Mantle Metasomatism and Kimberlite Ascent Indicated by Diffusion Profiles in Garnet Crystals from Peridotite Xenoliths. Earth Planet. Sci. Lett. 2018, 481, 143–153. [Google Scholar] [CrossRef]
  8. Deng, L.X.; Liu, Y.S.; Zong, K.Q.; Zhu, L.Y.; Hu, Z.C. Carbonate Metasomatism and Its Identification Characteristics in Mantle Peridotite. Earth Sci. 2019, 44, 1113–1127. (In Chinese) [Google Scholar]
  9. Xu, B.; Hou, Z.Q.; Griffin, W.L.; Yu, J.X.; Long, T.; Zhao, Y.; Wang, T.; Fu, B.; Belousova, E.; O’Reilly, S.Y. Apatite Halogens and Sr-O and Zircon Hf-O Isotopes: Recycled Volatiles in Jurassic Porphyry Ore Systems in Southern Tibet. Chem. Geol. 2022, 605, 120924. [Google Scholar] [CrossRef]
  10. Xu, B.; Hou, Z.-Q.; Griffin, W.L.; Lu, Y.; Belousova, E.; Xu, J.-F.; O’Reilly, S.Y. Recycled Volatiles Determine Fertility of Porphyry Deposits in Collisional Settings. Am. Mineral. 2021, 106, 656–661. [Google Scholar] [CrossRef]
  11. Deng, J.; Wang, C.; Bagas, L.; Santosh, M.; Yao, E. Crustal Architecture and Metallogenesis in the South-Eastern North China Craton. Earth-Sci. Rev. 2018, 182, 251–272. [Google Scholar] [CrossRef]
  12. Deng, J.; Liu, X.; Wang, Q.; Dilek, Y.; Liang, Y. Isotopic Characterization and Petrogenetic Modeling of Early Cretaceous Mafic Diking—Lithospheric Extension in the North China Craton, Eastern Asia. GSA Bulletin 2017, 129, 1379–1407. [Google Scholar] [CrossRef]
  13. Deng, J.; Wang, C.; Bagas, L.; Carranza, E.J.M.; Lu, Y. Cretaceous–Cenozoic Tectonic History of the Jiaojia Fault and Gold Mineralization in the Jiaodong Peninsula, China: Constraints from Zircon U–Pb, Illite K–Ar, and Apatite Fission Track Thermochronometry. Miner Deposita 2015, 50, 987–1006. [Google Scholar] [CrossRef]
  14. Wang, W.Y.; Sueno, S.; Takahashi, E.; Yurimoto, H.; Gasparik, T. Enrichment Processes at the Base of the Archean Lithospheric Mantle: Observations from Trace Element Characteristics of Pyropic Garnet Inclusions in Diamonds. Contrib. Mineral. Petrol. 2000, 139, 720–733. [Google Scholar] [CrossRef]
  15. Doucet, L.S.; Ionov, D.A.; Golovin, A.V. The Origin of Coarse Garnet Peridotites in Cratonic Lithosphere: New Data on Xenoliths from the Udachnaya Kimberlite, Central Siberia. Contrib. Mineral. Petrol. 2013, 165, 1225–1242. [Google Scholar] [CrossRef]
  16. Shu, Q.; Brey, G.P. Ancient Mantle Metasomatism Recorded in Subcalcic Garnet Xenocrysts: Temporal Links between Mantle Metasomatism, Diamond Growth and Crustal Tectonomagmatism. Earth Planet. Sci. Lett. 2015, 418, 27–39. [Google Scholar] [CrossRef]
  17. Nkere, B.J.; Janney, P.E.; Tinguely, C. Cr-Poor and Cr-Rich Clinopyroxene and Garnet Megacrysts from Southern African Group 1 and Group 2 Kimberlites: Clues to Megacryst Origins and Their Relationship to Kimberlites. Lithos 2021, 396–397, 106231. [Google Scholar] [CrossRef]
  18. Xu, B.; Hou, Z.-Q.; Griffin, W.L.; Zheng, Y.-C.; Wang, T.; Guo, Z.; Hou, J.; Santosh, M.; O’Reilly, S.Y. Cenozoic Lithospheric Architecture and Metallogenesis in Southeastern Tibet. Earth Sci. Rev. 2021, 214, 103472. [Google Scholar] [CrossRef]
  19. Deng, J.; Liu, X.; Wang, Q.; Pan, R. Origin of the Jiaodong-Type Xinli Gold Deposit, Jiaodong Peninsula, China: Constraints from Fluid Inclusion and C–D–O–S–Sr Isotope Compositions. Ore Geol. Rev. 2015, 65, 674–686. [Google Scholar] [CrossRef]
  20. Deng, J.; Wang, Q. Gold Mineralization in China: Metallogenic Provinces, Deposit Types and Tectonic Frame-work. Gondwana Res. 2016, 36, 219–274. [Google Scholar] [CrossRef]
  21. Griffin, W.L.; Shee, S.R.; Ryan, C.G.; Win, T.T.; Wyatt, B.A. Harzburgite to Lherzolite and Back Again: Metasomatic Processes in Ultramafic Xenoliths from the Wesselton Kimberlite, Kimberley, South Africa. Contrib. Mineral. Petrol. 1999, 134, 232–250. [Google Scholar] [CrossRef]
  22. Rudnick, R.L.; McDonough, W.F.; Chappell, B.W. Carbonatite Metasomatism in the Northern Tanzanian Mantle: Petrographic and Geochemical Characteristics. Earth Planet. Sci. Lett. 1992, 114, 463–475. [Google Scholar] [CrossRef]
  23. Zhu, R.Z.; Ni, P.; Ding, J.Y.; Wang, G.G.; Fan, M.S.; Li, S.N. Metasomatic Processes in the Lithospheric Mantle beneath the No.30 Kimberlite (Wafangdian Region, North China Craton). Can. Mineral. 2019, 57, 499–517. [Google Scholar] [CrossRef]
  24. Anton, L.R.; Christel, T.; Michel, G. Eclogite and Garnet Pyroxenite Xenoliths from Kimberlites Emplaced Along the Southern Margin of the Kaapvaal Craton, Southern Africa: Mantle or Lower Crustal Fragments? J. Petrol. 2020, 61, egaa040. [Google Scholar] [CrossRef]
  25. Shaikh, A.M.; Tappe, S.; Bussweiler, Y.; Patel, S.C.; Ravi, S.; Bolhar, R.; Viljoen, F. Clinopyroxene and Garnet Mantle Cargo in Kimberlites as Probes of Dharwar Craton Architecture and Geotherms, with Implications for Post-1·1 Ga Lithosphere Thinning Events Beneath Southern India. J. Petrol. 2021, 61, egaa087. [Google Scholar] [CrossRef]
  26. Sobolev, N.V.; Lavrent’ev, Y.G.; Pokhilenko, N.P.; Usova, L.V. Chrome-Rich Garnets from the Kimberlites of Yakutia and Their Parageneses. Contrib. Mineral. Petrol. 1973, 40, 39–52. [Google Scholar] [CrossRef]
  27. Dawson, J.B.; Stephens, W.E. Statistical Classification of Garnets from Kimberlite and Associated Xenoliths. J. Petrol. 1975, 83, 589–607. [Google Scholar] [CrossRef]
  28. Gurney, J.J.; Glover, J.E.; Harris, P.G. A Correlation between Garnets and Diamonds, Kimberlite Occurrence and Origin: A Basis for Conceptual Models in Exploration; Geology Department, University Extension, University of Western Australia Publishing: Crawley, Australia, 1984; Volume 8, pp. 143–166. [Google Scholar]
  29. Grütter, H.S.; Gurney, J.J.; Menzies, A.H.; Winter, F. An Updated Classification Scheme for Mantle-Derived Garnet, for Use by Diamond Explorers. Lithos 2004, 77, 841–857. [Google Scholar] [CrossRef]
  30. Zhang, A.D.; Xie, X.L.; Guo, L.H.; Zhou, J.X.; Xu, D.H.; Wang, W.Y.; Liu, Y.L.; Chen, Y.Z. Indication Minerals for Diamonds and the Data Base; Beijing Science and Technology Press: Beijing, China, 1991; pp. 71–75. (In Chinese) [Google Scholar]
  31. Chi, J.S.; Lu, F.X. The Study of Formation Conditions of Primary Diamond Deposits in China; China University Geosciences Press: Wuhan, China, 1996; pp. 43–47. (In Chinese) [Google Scholar]
  32. Yang, L.Q.; Deng, J.; Wang, Z.L.; Guo, L.N.; Li, R.H.; Groves, D.I.; Danyushevsky, L.V.; Zhang, C.; Zheng, X.L.; Zhao, H. Relationships Between Gold and Pyrite at the Xincheng Gold Deposit, Jiaodong Peninsula, China: Implications for Gold Source and Deposition in a Brittle Epizonal Environment. Econ. Geol. 2016, 111, 105–126. [Google Scholar] [CrossRef]
  33. Yang, L.Q.; Deng, J.; Wang, Z.L.; Zhang, L.; Goldfarb, R.J.; Yuan, W.M.; Weinberg, R.F.; Zhang, R.Z. Thermochronologic Constraints on Evolution of the Linglong Metamorphic Core Complex and Implications for Gold Mineralization: A Case Study from the Xiadian Gold Deposit, Jiaodong Peninsula, Eastern China. Ore Geol. Rev. 2016, 72, 165–178. [Google Scholar] [CrossRef]
  34. Deng, J.; Wang, Q.F.; Santosh, M.; Liu, X.F.; Liang, Y.Y.; Yang, L.Q.; Zhao, R.; Yang, L. Remobilization of Metasomatized Mantle Lithosphere: A New Model for the Jiaodong Gold Province, Eastern China. Min. Depos. 2020, 55, 257–274. [Google Scholar] [CrossRef]
  35. Wang, Z.C.; Cheng, H.; Zong, K.Q.; Geng, X.L.; Liu, Y.S.; Yang, J.H.; Wu, F.Y.; Becker, H.; Foley, S.; Wang, C.Y. Metasomatized Lithospheric Mantle for Mesozoic Giant Gold Deposits in the North China Craton. Geology 2020, 48, 169–173. [Google Scholar] [CrossRef]
  36. Zhang, L.; Weinberg, R.F.; Yang, L.Q.; Groves, D.I.; Sai, S.X.; Matchan, E.; Phillips, D.; Kohn, B.P.; Miggins, D.P.; Liu, Y.; et al. Mesozoic Orogenic Gold Mineralization in the Jiaodong Peninsula, China: A Focused Event at 120 ± 2 Ma During Cooling of Pregold Granite Intrusions. Econ. Geol. 2020, 115, 415–441. [Google Scholar] [CrossRef]
  37. Song, M.C.; Yu, X.S.; Song, Y.X.; Xiao, B.J.; Zhou, D.S.; Gao, C.S.; Feng, A.P. Types, sources, and regional crust-mantle evolution background of diamonds in the western Shandong Province. Acta Geosci. Sinica. 2020, 94, 2606–2625. (In Chinese) [Google Scholar]
  38. Deng, J.; Qiu, K.F.; Wang, Q.F.; Goldfarb, R.; Yang, L.Q.; Zi, J.W.; Geng, J.Z.; Ma, Y. In-situ dating of hydrothermal monazite and implications on the geodynamic controls of ore formation in the Jiaodong gold province, eastern China. Econ. Geol. 2020, 115, 671–685. [Google Scholar] [CrossRef]
  39. Chi, J.S.; Lu, F.X. Kimberlites from the North China Craton and Nature of Palaeozoic Lithospheric Mantle; Science Press: Beijing, China, 1996; pp. 16–21. (In Chinese) [Google Scholar]
  40. Zhang, H.F.; Menzies, M.A.; Lu, F.X.; Zhou, X.H. Major and Trace Element Studies on Garnets from Palaeozoic Kimberlite-Borne Mantle Xenoliths and Megacrysts from the North China Craton. Sci. China (Ser. D) 2000, 43, 423–430. [Google Scholar] [CrossRef]
  41. Chi, G.C.; Wu, Y.; Hu, J.F. The Characteristics and Classification of Garnets from Kimberlite in Mengyin, Shandong Province. Acta Petrol. Mineral. 2014, 33, 877–884. (In Chinese) [Google Scholar]
  42. Zhao, X.F.; Chu, Z.Y. A Study of Diamond Indicative Minerals in The Depth and Periphery of Xiyu, Mengyin County, Shandong Province: Metallogenic Properties of Kimberlite Predicted by Diamond Indicating Minerals. Geol. Bull. China 2019, 38, 121–131. (In Chinese) [Google Scholar]
  43. Lu, F.X. Kimberlite and Diamond. Nat. Mag. 2008, 30, 63–66. (In Chinese) [Google Scholar]
  44. Zhang, H.F.; Lu, F.X.; Zhao, L.; Menzies, M.A.; Mattey, D.P.; Liang, S.Y. Carbon Isotopes in China Natural Diamonds. Earth Sci. —J. China Univ. Geosci. 2009, 34, 37–42. (In Chinese) [Google Scholar]
  45. Deng, J.; Yang, L.Q.; Groves, D.I.; Zhang, L.; Qiu, K.F.; Wang, Q.F. An Integrated Mineral System Model for the Gold Deposits of the Giant Jiaodong Province, Eastern China. Earth Sci. Rev. 2020, 208, 103274. [Google Scholar] [CrossRef]
  46. Lv, Q.; Liu, F.; Chu, Z.Y.; Ge, Y.J.; Liu, X.; Jiao, Y.X. The Mineralogical Characteristics and Comparison of Diamonds from the Three Kimberlite Belts in Mengyin, Shandong Province. Acta Geology Sinica. 2022, 96, 4. (In Chinese) [Google Scholar]
  47. Yang, Z.J.; Huang, S.S.; Chen, Y.M.; Lei, X.Y.; Li, X.X.; Zeng, X. Characteristics and Their Geological Significances of Spinel Minerals of Kimberlite in Mengyin, Shandong Province. Bull. Mineral. Petrol. Geochem. 2018, 37, 2. (In Chinese) [Google Scholar]
  48. Chu, Z.Y. Study on Characteristics and Diamondiferous Significance of the Mengyin Kimberlite in Shandong Province, China. Master’s Thesis, China University of Geosciences (Beijing), Beijing, China, 2019. (In Chinese). [Google Scholar]
  49. Zhang, P.Q. Origin of Kimberlitic Pipes in Shandong Province. Ph.D. Thesis, China University of Geosciences (Beijing), Beijing, China, 2006. (In Chinese). [Google Scholar]
  50. Wu, Y.F. The Study on Shengli No.1 Pipe Mengyin Shandong Kimberlite Mineralogical Characteristics. Master’s Thesis, China University of Geosciences (Beijing), Beijing, China, 2013. (In Chinese). [Google Scholar]
  51. Xiang, Z.J.; Yang, Z.J.; Lei, X.Y. The Microfabrics of Phlogopite from the Mengyin Kimberlites and their Implications to the Magma Evolution. Bull. Mineral. Petrol. Geochem. 2020, 39, 1. (In Chinese) [Google Scholar]
  52. Sun, S.S.; McDonough, W.F. Chemical and Isotopic Systematics of Ocean Basalts: Implications for Mantle Composition and Processes, in Magmatism in the Ocean Basins. Geol. Soc. Lond. Spec. Publ. 1989, 423, 13–345. [Google Scholar]
  53. Kelemen, P.B.; Hart, S.R.; Bernstein, S. Silica Enrichment in the Continental Upper Mantle via Melt/Rock Reaction. Earth Planet Sci. Lett. 1998, 164, 387–406. [Google Scholar] [CrossRef]
  54. Herzberg, C. Geodynamic Information in Peridotite Petrology. J. Petrol. 2004, 45, 2507–2530. [Google Scholar] [CrossRef]
  55. Gibson, S.A.; Malarkey, J.; Day, J.A. Melt Depletion and Enrichment beneath the Western Kaapvaal Craton: Evidence from Finsch Peridotite Xenoliths. J. Petrol. 2008, 49, 1817–1852. [Google Scholar] [CrossRef]
  56. Gibson, S.A.; McMahon, S.C.; Day, J.A.; Dawson, J.B. Highly Refractory Lithospheric Mantle beneath the Tanzanian Craton: Evidence from Lashaine Pre-Metasomatic Garnet-Bearing Peridotites. J. Petrol. 2013, 54, 1503–1546. [Google Scholar] [CrossRef]
  57. Simon, N.S.C.; Carlson, R.W.; Pearson, D.G.; Davies, G.R. The Origin and Evolution of the Kaapvaal Cratonic Lithospheric Mantle. J. Petrol. 2007, 48, 589–625. [Google Scholar] [CrossRef]
  58. Stachel, T.; Aulbach, S.; Brey, G.P.; Harris, J.W.; Leost, I.; Tappert, R.; Viljoen, K.S. (Fanus) The Trace Element Composition of Silicate Inclusions in Diamonds: A Review. Lithos 2004, 77, 1–19. [Google Scholar] [CrossRef]
  59. Yaxley, G.M.; Crawford, A.J.; Green, D.H. Evidence for Carbonatite Metasomatism in Spinel Peridotite Xenoliths from Western Victoria, Australia. Earth Planet Sci. Lett. 1991, 107, 305–317. [Google Scholar] [CrossRef]
  60. Bell, K.; Blenkinsop, J.; Cole, T.J.S.; Menagh, D.P. Evidence from Sr Isotopes for Long-Lived Heterogeneities in the Upper Mantle. Nature 1982, 298, 251–253. [Google Scholar] [CrossRef]
  61. Woolley, A.R.; Kjarsgaard, B.A. Carbonatite Occurrences of the World: Map and Database. Geol. Surv. Can. 2008, 5796, 1–28. [Google Scholar]
  62. Haggerty, S.E. Super kimberlites: A Geodynamic Diamond Window to the Earth’s Core. Earth Planet Sci. Lett. 1994, 122, 57–69. [Google Scholar] [CrossRef]
  63. Dalton, J.A.; Presnall, D.C. The Continuum of Primary Carbonatitic-Kimberlitic Melt Compositions in Equilibrium with Lherzolite: Data from the System CaO-MgO-Al2O3-SiO2-CO2 at 6 GPa. J. Petrol. 1998, 39, 1953–1964. [Google Scholar] [CrossRef]
  64. Zhang, H.F.; Yang, Y.H. Emplacement Age and Sr-Nd-Hf Isotopic Characteristics of the Diamondiferous Kimberlites from the Eastern North China Craton. Acta Petrol. Sin. 2007, 23, 285–294. (In Chinese) [Google Scholar]
  65. Peng, P.; Bleeker, W.; Ernst, R.E.; Söderlund, U.; McNicoll, V. U–Pb Baddeleyite Ages, Distribution and Geochemistry of 925Ma Mafic Dykes and 900Ma Sills in the North China Craton: Evidence for a Neoproterozoic Mantle Plume. Lithos 2011, 127, 210–221. [Google Scholar] [CrossRef]
  66. Yang, Y.H.; Wu, F.Y.; Wilde, S.A.; Liu, X.M.; Zhang, Y.B.; Xie, L.W.; Yang, J.H. In Situ Perovskite Sr–Nd Isotopic Constraints on the Petrogenesis of the Ordovician Mengyin Kimberlites in the North China Craton. Chem. Geol. 2009, 264, 24–42. [Google Scholar] [CrossRef]
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Figure 1. (a) The location of the Mengyin area in North China Craton. Modified from [45]. (b) Geological map of the Mengyin region and kimberlite location, modified from [46]. The blue dashed squares represent three main rock belts: Changmazhuang rock belt, Xiyu rock belt, and Poli rock belt.
Figure 1. (a) The location of the Mengyin area in North China Craton. Modified from [45]. (b) Geological map of the Mengyin region and kimberlite location, modified from [46]. The blue dashed squares represent three main rock belts: Changmazhuang rock belt, Xiyu rock belt, and Poli rock belt.
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Figure 2. (a,b) The picture of sample SL1-1 and sample SL5-2, collected from the Shengli No. 1 kimberlite pipe. (c,d) Scanning image of the sample under single polarized light. (e,f) Photographs of samples under single polarized light. (g,h) Backscattered images of samples.
Figure 2. (a,b) The picture of sample SL1-1 and sample SL5-2, collected from the Shengli No. 1 kimberlite pipe. (c,d) Scanning image of the sample under single polarized light. (e,f) Photographs of samples under single polarized light. (g,h) Backscattered images of samples.
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Figure 3. (a) Garnet Cr2O3 variations of Shengli No. 1 kimberlite pipe, the base map is from [26]. Wh is wehrlite paragenesis. Lz is lherzolite paragenesis. Hz is harzburgite paragenesis. (b) Garnet TiO2-Cr2O3 variations of Shengli No. 1 kimberlite pipe. The data of garnet inclusion in diamond are from [14].
Figure 3. (a) Garnet Cr2O3 variations of Shengli No. 1 kimberlite pipe, the base map is from [26]. Wh is wehrlite paragenesis. Lz is lherzolite paragenesis. Hz is harzburgite paragenesis. (b) Garnet TiO2-Cr2O3 variations of Shengli No. 1 kimberlite pipe. The data of garnet inclusion in diamond are from [14].
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Figure 4. (a) The diagram illustrates the evolutionary changes in the CaO-Cr2O3 composition of garnets during two stages of metasomatism, adapted from [1]. Trend 1 represents carbonatitic metasomatism, while Trend 2 corresponds to kimberlitic metasomatism (blue lines represent metasomatic evolution). Blue arrows represent Trend 1 and Trend 2. (b–f) The diagram depicts chondrite-normalized rare earth element (REE) patterns (based on [52]) for garnet xenocrysts collected from the Shengli No. 1 kimberlite pipe in the Mengyin region. The data on garnet inclusions in diamonds from Mengyin are sourced from [14].
Figure 4. (a) The diagram illustrates the evolutionary changes in the CaO-Cr2O3 composition of garnets during two stages of metasomatism, adapted from [1]. Trend 1 represents carbonatitic metasomatism, while Trend 2 corresponds to kimberlitic metasomatism (blue lines represent metasomatic evolution). Blue arrows represent Trend 1 and Trend 2. (b–f) The diagram depicts chondrite-normalized rare earth element (REE) patterns (based on [52]) for garnet xenocrysts collected from the Shengli No. 1 kimberlite pipe in the Mengyin region. The data on garnet inclusions in diamonds from Mengyin are sourced from [14].
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Figure 5. (a) Garnet (Sm/Er)N vs. Cr2O3 of Shengli No. 1 kimberlite pipe in Mengyin. (b) Garnet (Tm/Yb)N vs. Cr2O3 of Shengli No. 1 kimberlite pipe in Mengyin.
Figure 5. (a) Garnet (Sm/Er)N vs. Cr2O3 of Shengli No. 1 kimberlite pipe in Mengyin. (b) Garnet (Tm/Yb)N vs. Cr2O3 of Shengli No. 1 kimberlite pipe in Mengyin.
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Figure 6. Zr versus TiO2 plots of garnet xenocrysts from Shengli No. 1 kimberlite pipe, Mengyin. The base map is from [21]. Garnet inclusions data in diamonds are from [14].
Figure 6. Zr versus TiO2 plots of garnet xenocrysts from Shengli No. 1 kimberlite pipe, Mengyin. The base map is from [21]. Garnet inclusions data in diamonds are from [14].
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Figure 7. (a) (Sm/Er)N versus Ti/Eu plots of garnet xenocrysts from Shengli No. 1 kimberlite pipe, Mengyin. The base map is from [23]. (b) Zr/Hf versus Ti/Eu plots of garnet xenocrysts from Shengli No. 1 kimberlite pipe, Mengyin. The base map is from [16]. The gray pentagram is PM, which means primitive mantle. Garnet inclusions data in diamonds are from [14].
Figure 7. (a) (Sm/Er)N versus Ti/Eu plots of garnet xenocrysts from Shengli No. 1 kimberlite pipe, Mengyin. The base map is from [23]. (b) Zr/Hf versus Ti/Eu plots of garnet xenocrysts from Shengli No. 1 kimberlite pipe, Mengyin. The base map is from [16]. The gray pentagram is PM, which means primitive mantle. Garnet inclusions data in diamonds are from [14].
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Table 1. The feature of garnet xenocrysts from Shengli No. 1 kimberlite pipe.
Table 1. The feature of garnet xenocrysts from Shengli No. 1 kimberlite pipe.
SampleParticle SizeShapeFragmentation DegreeAlteration Degree
SL1-12.4 mmEllipticityWeakModerate
SL1-21.6 mmGranulationStrongStrong
SL5-18 mmEllipticityStrongModerate
SL5-21.8 mmGranulationStrongStrong
SL7-12 mmEllipticityWeakModerate
SL11-10.4 mmGranulationModerateStrong
SL12-10.03 mmGranulationWeakStrong
SLJ5-24.5 mmRoundnessModerateModerate
Table 2. Major elements of garnet xenocrysts from Shengli No. 1 kimberlite pipe (wt.%).
Table 2. Major elements of garnet xenocrysts from Shengli No. 1 kimberlite pipe (wt.%).
Garnet Sample Cr2O3MgOAl2O3CaOFeOTiO2
SL1-1Min.6.93 19.68 17.37 5.39 7.12 0.17
Max.7.64 20.66 17.86 5.78 7.54 0.34
SD.0.18 0.30 0.17 0.13 0.13 0.05
n = 11Av.7.14 20.29 17.65 5.60 7.32 0.23
SL1-2Min.5.05 20.64 18.41 4.73 6.58 0.39
Max.5.41 21.81 20.16 4.95 7.20 0.52
SD.0.10 0.38 0.54 0.08 0.21 0.04
n = 12Av.5.27 21.38 19.04 4.85 6.80 0.46
SL5-1Min.7.13 21.11 17.06 4.76 5.77 0.35
Max.7.51 22.53 17.98 5.11 6.27 0.88
SD.0.11 0.46 0.32 0.11 0.15 0.15
n = 12Av.7.25 21.51 17.72 4.92 6.10 0.54
SL5-2Min.5.26 20.01 18.93 5.05 6.82 0.00
Max.5.72 21.26 20.07 5.42 7.39 0.03
SD.0.13 0.43 0.34 0.08 0.19 0.01
n = 16Av.5.49 20.35 19.70 5.27 7.18 0.01
SL7-1Min.4.14 20.62 18.41 4.78 7.01 0.93
Max.4.52 21.91 19.62 5.04 7.73 1.14
SD.0.11 0.46 0.49 0.10 0.24 0.08
n = 12Av.4.32 21.17 18.99 4.91 7.44 1.01
SL11-1Min.5.01 20.51 18.12 4.76 6.65 0.82
Max.5.27 21.93 19.72 5.05 7.23 1.09
SD.0.10 0.47 0.70 0.09 0.22 0.08
n = 7Av.5.12 21.15 18.83 4.90 6.94 0.96
SL12-1Min.4.12 21.30 19.51 4.68 7.15 0.44
Max.4.40 21.48 20.07 4.82 7.49 0.51
SD.0.10 0.08 0.24 0.05 0.14 0.03
n = 5Av.4.26 21.37 19.72 4.76 7.31 0.48
SLJ5-2Min.4.95 20.80 18.93 5.31 6.56 0.00
Max.5.39 21.36 19.85 5.47 6.95 0.06
SD.0.11 0.14 0.27 0.06 0.12 0.02
n = 13Av.5.13 21.12 19.48 5.39 6.85 0.03
Table 3. Trace elements of garnet xenocrysts from Shengli No. 1 kimberlite pipe (ppm).
Table 3. Trace elements of garnet xenocrysts from Shengli No. 1 kimberlite pipe (ppm).
Garnet Sample SrNiZrHfYLaCePrNdSmEu
SL1-1Min.0.34 52.95 9.84 0.17 3.51 0.03 0.58 0.15 1.09 0.43 0.26
Max.0.74 59.66 47.10 0.82 4.20 0.08 0.80 0.25 2.77 1.28 0.47
SD.0.16 2.21 14.02 0.23 0.25 0.02 0.07 0.04 0.60 0.34 0.07
n = 8AV.0.53 55.55 22.98 0.42 3.81 0.06 0.69 0.20 1.80 0.78 0.35
SL1-2Min.0.45 79.97 31.49 0.59 12.19 0.08 0.32 0.10 0.70 0.72 0.31
Max.0.64 103.56 32.62 0.79 12.71 0.20 0.49 0.14 1.12 0.85 0.40
SD.0.08 10.04 0.51 0.09 0.20 0.05 0.07 0.02 0.15 0.05 0.03
n = 5AV.0.51 92.07 32.04 0.70 12.51 0.15 0.41 0.12 0.94 0.79 0.35
SL5-1Min.0.98 113.69 25.86 0.56 5.16 0.10 0.94 0.28 2.49 1.22 0.51
Max.1.20 120.77 46.97 0.85 5.92 0.17 1.13 0.42 3.42 1.86 0.66
SD.0.08 2.10 7.79 0.09 0.22 0.02 0.06 0.04 0.24 0.18 0.06
n = 11AV.1.10 116.19 32.08 0.71 5.44 0.12 1.06 0.35 2.99 1.47 0.58
SL5-2Min.0.60 59.33 1.05 0.00 1.29 0.04 0.57 0.20 1.69 0.27 0.03
Max.0.75 67.05 11.16 0.20 1.49 0.08 0.73 0.27 2.40 0.78 0.20
SD.0.05 2.46 3.02 0.05 0.05 0.01 0.05 0.02 0.18 0.14 0.05
n = 14AV.0.70 61.64 3.48 0.06 1.43 0.06 0.64 0.23 1.98 0.42 0.08
SL7-1Min.0.74 111.08 74.46 1.56 6.80 0.05 0.64 0.20 1.62 1.20 0.41
Max.0.92 116.78 112.12 2.93 8.50 0.10 0.78 0.27 2.47 1.54 0.64
SD.0.07 1.74 13.28 0.47 0.63 0.02 0.04 0.02 0.25 0.11 0.08
n = 11AV.0.86 112.94 91.60 2.06 7.47 0.08 0.70 0.23 2.20 1.36 0.56
SL11-1Min.1.01 125.33 52.97 0.86 5.69 0.14 0.91 0.24 2.59 1.18 0.36
Max.19.01 1015.15 78.44 1.40 7.76 32.64 13.80 1.07 4.92 1.35 0.47
SD.10.33 513.65 13.03 0.29 1.13 18.69 7.31 0.48 1.33 0.09 0.06
n = 3AV.7.08 422.04 67.30 1.19 6.99 11.06 5.36 0.52 3.38 1.25 0.41
SLJ5-2Min.0.67 62.48 6.27 0.10 1.59 0.05 0.62 0.24 2.23 0.36 0.10
Max.0.89 97.62 30.65 0.55 1.97 0.17 0.89 0.31 2.96 1.20 0.38
SD.0.07 10.95 6.67 0.15 0.11 0.04 0.08 0.02 0.21 0.26 0.08
n = 11AV.0.79 72.42 16.76 0.31 1.67 0.09 0.73 0.27 2.57 0.90 0.24
Garnet Sample EuGdTbDyHoErTmYbLuTi/EuZr/Hf
SL1-1Min.0.26 0.67 0.11 0.66 0.13 0.37 0.06 0.54 0.09 5.70 0.53
Max.0.47 1.40 0.18 0.92 0.18 0.45 0.08 0.73 0.12 6.87 0.82
SD.0.07 0.26 0.03 0.08 0.02 0.03 0.01 0.06 0.01 0.43 0.10
n = 8AV.0.35 0.97 0.14 0.77 0.16 0.40 0.07 0.61 0.10 6.26 0.67
SL1-2Min.0.31 1.00 0.19 1.72 0.40 1.49 0.24 1.61 0.29 5.91 0.72
Max.0.40 1.28 0.27 2.03 0.51 1.69 0.27 2.06 0.36 7.77 0.94
SD.0.03 0.11 0.03 0.11 0.04 0.08 0.02 0.20 0.03 0.77 0.11
n = 5AV.0.35 1.17 0.23 1.88 0.46 1.56 0.26 1.88 0.32 6.72 0.82
SL5-1Min.0.51 1.49 0.18 1.05 0.18 0.38 0.06 0.36 0.05 8.79 0.69
Max.0.66 1.77 0.27 1.36 0.23 0.57 0.08 0.61 0.09 15.66 1.24
SD.0.06 0.09 0.03 0.11 0.02 0.05 0.01 0.07 0.01 1.85 0.18
n = 11AV.0.58 1.63 0.21 1.20 0.20 0.48 0.07 0.46 0.07 12.17 0.93
SL5-2Min.0.03 0.06 0.01 0.05 0.04 0.19 0.03 0.49 0.11 1.99 0.22
Max.0.20 0.32 0.03 0.17 0.06 0.31 0.08 0.71 0.15 2.98 0.60
SD.0.05 0.08 0.01 0.03 0.01 0.04 0.01 0.06 0.01 0.24 0.11
n = 14AV.0.08 0.18 0.02 0.12 0.05 0.24 0.06 0.60 0.13 2.41 0.44
SL7-1Min.0.41 1.50 0.23 1.26 0.24 0.62 0.09 0.67 0.12 5.98 0.70
Max.0.64 2.26 0.34 1.94 0.36 0.83 0.13 1.17 0.16 10.64 0.99
SD.0.08 0.27 0.03 0.20 0.03 0.07 0.01 0.15 0.01 1.62 0.11
n = 11AV.0.56 1.82 0.28 1.55 0.28 0.72 0.11 0.89 0.14 8.61 0.80
SL11-1Min.0.36 0.98 0.18 1.06 0.24 0.67 0.09 0.62 0.12 9.13 0.77
Max.0.47 1.32 0.21 1.28 0.31 0.87 0.14 0.78 0.13 10.00 1.19
SD.0.06 0.18 0.02 0.12 0.03 0.11 0.03 0.08 0.01 0.48 0.22
n = 3AV.0.41 1.18 0.20 1.14 0.27 0.80 0.11 0.72 0.12 9.68 0.95
SLJ5-2Min.0.10 0.21 0.02 0.13 0.04 0.24 0.04 0.60 0.12 2.05 0.27
Max.0.38 0.86 0.08 0.35 0.08 0.33 0.08 0.80 0.17 2.65 0.52
SD.0.08 0.19 0.02 0.06 0.01 0.03 0.01 0.07 0.01 0.20 0.07
n = 11AV.0.24 0.45 0.04 0.20 0.06 0.29 0.06 0.69 0.15 2.42 0.43
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Wang, H.-S.; Yang, L.-Q.; Chu, Z.-Y.; Zhang, L.; Li, N.; He, W.-Y.; Zhang, Y.-N.; Wang, Y.-Q. Ancient Metasomatism in the Lithospheric Mantle, Eastern North China Craton: Insights from In-Situ Major and Trace Elements in Garnet Xenocrysts, Mengyin District. Minerals 2023, 13, 1106. https://doi.org/10.3390/min13081106

AMA Style

Wang H-S, Yang L-Q, Chu Z-Y, Zhang L, Li N, He W-Y, Zhang Y-N, Wang Y-Q. Ancient Metasomatism in the Lithospheric Mantle, Eastern North China Craton: Insights from In-Situ Major and Trace Elements in Garnet Xenocrysts, Mengyin District. Minerals. 2023; 13(8):1106. https://doi.org/10.3390/min13081106

Chicago/Turabian Style

Wang, Hao-Shuai, Li-Qiang Yang, Zhi-Yuan Chu, Liang Zhang, Nan Li, Wen-Yan He, Ya-Nan Zhang, and Yi-Qi Wang. 2023. "Ancient Metasomatism in the Lithospheric Mantle, Eastern North China Craton: Insights from In-Situ Major and Trace Elements in Garnet Xenocrysts, Mengyin District" Minerals 13, no. 8: 1106. https://doi.org/10.3390/min13081106

APA Style

Wang, H. -S., Yang, L. -Q., Chu, Z. -Y., Zhang, L., Li, N., He, W. -Y., Zhang, Y. -N., & Wang, Y. -Q. (2023). Ancient Metasomatism in the Lithospheric Mantle, Eastern North China Craton: Insights from In-Situ Major and Trace Elements in Garnet Xenocrysts, Mengyin District. Minerals, 13(8), 1106. https://doi.org/10.3390/min13081106

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