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Article

Metallogenic Epoch and Tectonic Setting of Saima Niobium Deposit in Fengcheng, Liaoning Province, NE China

by
Nan Ju
1,2,*,
Yun-Sheng Ren
1,
Sen Zhang
2,
Zhong-Wei Bi
2,
Lei Shi
2,
Di Zhang
2,
Qing-Qing Shang
1,
Qun Yang
1,
Zhi-Gao Wang
1,
Yu-Chao Gu
2,
Qiu-Shi Sun
2 and
Tong Wu
2
1
College of Earth Sciences, Jilin University, Changchun 130061, China
2
Shenyang Geological Survey, CGS, Shenyang 110034, China
*
Author to whom correspondence should be addressed.
Minerals 2019, 9(2), 80; https://doi.org/10.3390/min9020080
Submission received: 17 December 2018 / Revised: 14 January 2019 / Accepted: 24 January 2019 / Published: 29 January 2019
(This article belongs to the Special Issue Polymetallic Metallogenic System)
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Versions Notes

Abstract

:
The Saima deposit is a newly discovered niobium deposit which is located in the eastern of Liaoning Province, NE China. Its mineralization age and geochemical characteristics are firstly reported in this study. The Nb orebodies are hosted by the grey–brown to grass-green aegirine nepheline syenite. Detailed petrographical studies show that the syenite consists of orthoclase (~50%), nepheline (~30%), biotite (~15%) and minor arfvedsonite (~3%) and aegirine (~2%), with weak hydrothermal alteration dominated by silicification. In situ LA-ICP-MS zircon U-Pb dating indicates that the aegirine nepheline syenite was emplaced in the Late Triassic (229.5 ± 2.2 Ma), which is spatially, temporally and genetically related to Nb mineralization. These aegirine nepheline syenites have SiO2 contents in the range of 55.86–63.80 wt. %, low TiO2 contents of 0.36–0.64 wt. %, P2O5 contents of 0.04–0.11 wt. % and Al2O3 contents of more than 15 wt. %. They are characterized by relatively high (K2O + Na2O) values of 9.72–15.51 wt. %, K2O/Na2O ratios of 2.42–3.64 wt. % and Rittmann indexes (σ = [ω(K2O + Na2O)]2/[ω(SiO2 − 43)]) of 6.84–17.10, belonging to the high-K peralkaline, metaluminous type. These syenites are enriched in large ion lithophile elements (LILEs, e.g., Cs, Rb and Ba) and light rare earth elements (LREEs) and relatively depleted in high field strength elements (HFSEs, e.g., Nb, Zr and Ti) and heavy rare earth elements (HREEs), with transitional elements showing an obvious W-shaped distribution pattern. Based on these geochronological and geochemical features, we propose that the ore-forming intrusion associated with the Nb mineralization was formed under post-collision continental-rift setting, which is consistent with the tectonic regime of post-collision between the North China Craton and Paleo-Asian oceanic plate during the age in Ma for Indosinian (257–205 Ma). Intensive magmatic and metallogenic events resulted from partial melting of lithospheric mantle occurred during the post-collisional rifting, resulting in the development of large-scale Cu–Mo mineralization and rare earth deposits in the eastern part of Liaoning Province.

1. Introduction

China’s reserves of rare earth metals account for up to 87% of the world total, while the reserves of niobium metals are relatively scarce, which only account for 18.19% of the world [1]. Geological survey in recent years have shown that most of the niobium (Nb) and tantalum (Ta) deposits are distributed in south China, such as Hunan, Guangdong, Shanxi and particularly Jiangxi Province in which host the most abundant Nb and Ta resources. Minor similar deposits have been sporadically discovered in the Panzhihua-Xichang district, northern Xinjiang and Inner Mongolia [2]. In contrast, few Nb and Ta deposits had been discovered in NE China, which was attributed to the restricted prospecting and research at present. However, numerous rare earth deposits associated with alkali rocks represented by Ba’erzhe (inner Mongolia province) have been recently discovered in NE China [3] and rare metals such as Nb and Ta occurred in alkaline intrusive rocks have received extensive attention.
The Saima deposit, an niobium deposit with medium-scale prospecting potentials, is located about 2 km to the south of Saima town, Fengcheng city, Liaoning province. Nevertheless, systematic studies on the metallogenic of the newly discovered Saima niobium deposit remain inadequate. In this study, we present new in situ LA-ICP-MS zircon U-Pb geochronological data and whole-rock geochemical data for the ore-forming alkaline intrusive rocks to constrain the timing and origin of the niobium mineralization and in particular, to shed light on the tectonic environment of regional deposition by the views of geological characteristics of the Saima deposit. Moreover, this study provides a scientific basis for further mineral prospecting and future prospecting of new rare earth deposits in NE China.

2. Geological Setting and Ore Deposit Geology

The Saima deposit is located in the intersection of the Taizihe–Hunjiang fault depression and Yingkou–Kuandian uplift in the Liaodong Massif, northeast of the North China Craton. Stratigraphic units are dominated by the Neoproterozoic, Cambrian–Ordovician, Jurassic and Quaternary alluvium. Massive Late Archean to Mesozoic granitic intrusions are exposed in the region, with particularly intensive magmatism during Late Triassic and Jurassic. Alkaline rocks closely related to the rare earth deposits are distributed along the intersection between the E–W-trending fault and NNE–SSW-trending fault. This alkaline rock belt extends about 40 km from east to west, with the width of 15 km, covering an area of about 200 km2. These rocks occurred as small stocks and apophysis and intruded into the Pre-Ordovician formations, showing angular unconformity contact with the overlying Jurassic strata. Four alkaline intrusions and abundant alkaline volcanic-subvolcanic rocks constitute the alkaline rock belt, with their alkalis gradually increasing from east to west and rock types changing from syenite–miascite (biotite–nepheline) to aegirine nepheline syenite. Regional faults are dominated by the E–W-trending faults, accompanied by the NE–SW-trending, NW–SE-trending and NNE–SSW-trending faults. The Saima deposit is located in the intersection of EW-trending fault and NE–SW-trending fault (Figure 1a), as these faults acted as the conduits for the migration and enrichment of ore-forming elements and provided favorable conditions for the formation of an alkaline rock type niobium deposit.
The strata in the Saima district consist of the Lower Proterozoic Gaixian Formation and Dashiqiao Formation, the Upper Proterozoic Xihe Group and Cambrian, Ordovician and Jurassic formations. Intense magmatism developed in the Saima district, including the Proterozoic magmatic rocks exposed in the eastern portion of the district and the Mesozoic magmatic rocks exposed in the western part. The Mesozoic magmatic rocks composed of Fengcheng alkaline intrusion as well as Nanda and Beida granitic intrusions, are controlled by the regional EW-trending faults. The ore-forming alkaline rocks occurred as dikes and stocks along the EW-trending structural zone and are characterized by medium- to fine-grained and pegmatitic textures, which had been interpreted to be the intrusive and flooding products of the Indosinian movement. These rocks are dominated by the aegirine nepheline syenite, accompanied by biotite-bearing aegirine nepheline syenite, black aegirine nepheline syenite, black grenadine syenite, miascite and green or grass-green aegirine nepheline syenite. They belong to the higher K2O, lower Na2O, alkaline to peralkaline series. The rare earth mineralization mainly occurred in the green, grass-green and grey–brown aegirine nepheline syenite. It develops EW-, NS-, NE–SW- and NW–SE-trending faults in the Saima district, with the NE–SW-trending faults as the ore-controlling faults [4,5] (Figure 1b). Extensive wall-rock alteration including microclinization, nephelinization, Na-zeolitization and carbonatization are well developed in the Saima deposit. Various kinds of primary nepheline syenite have been extensively altered to syenite, forming the main part of the Saima alkaline intrusion. The Nb and Ta mineralization was closely related to the nephelinization and Ca-nephelinization.
Currently, eight orebodies have been found in the Saima district, which mainly occurred in grey–brown to grass-green aegirine nepheline syenite. The No. I and II orebodies are about 500 m and 160 m long, with the width of 6 m and 18 m, respectively. Most of the orebodies are stratiform or lenticular, inclined to 45–115° and dip at 25–75°, with the maximum thickness up to 40 m (Figure 2). Fergusonite (YNbO4) and brocenite are the dominant ore minerals with high Nb grades of 0.03–0.06%, Ce grades of about 0.1%. Gangue minerals include nepheline, aegirine, rutile and pyrite. There is no sharp boundary between the orebodies and wall-rocks but rather a gradual transitional relationship. The rare earth ores show lamellated, cataclastic and subhedral pegmatitic textures and veined-disseminated structures.

3. Petrography and Analytical Methods

3.1. Petrographic Features

Samples analyzed in this study were collected from the No. II orebody in the Saima district (Figure 1). No (ore) mineralization and alteration had been distinguished in the sample SMB1 and it was considered as the original ore-forming rock. Thin sections were made from these samples and subsequently observed by using an OLYMPUS microscope at the Laboratory of Rock-mineral Determination, Jilin University. Detailed petrographic studies indicate that the ore-forming rocks are mainly medium-coarse grained aegirine nepheline syenite composed of subhedral-anhedral orthoclase (~50%) with carlsbad twinning, nepheline (~30%) with tabular or granular textures, biotite (~10%) partly replaced by nepheline, aegirine (~7%) and arfvedsonite (~3%; Figure 3). The aegirine nepheline syenites are in conformable and direct contact with the orebodies as shown in sketch map of TCG10-3 exploratory trench (Figure 2). Combined with the distribution characteristics of orebodies in the deposit scale (Figure 1), it is suggested that the aegirine nepheline syenite is spatially, temporally and genetically related to Nb mineralization.

3.2. Analytical Methods

3.2.1. Zircon LA-ICP-MS U-Pb Dating

Sample SMN1 collected from the aegirine nepheline syenite in the Saima district was selected for zircon U–Pb dating. Zircons were extracted using conventional heavy liquid and magnetic separation techniques and then handpicked under a binocular microscope at the Langfang Regional Geological Survey, Hebei Province, China. Their transmitted and reflected light images were obtained using a standard polarizing microscope and cathodoluminescence (CL) images were obtained using a JEOL scanning electron microscope (JEOL, Tokyo, Japan). LA-ICP-MS zircon U-Pb analyses were performed using an Agilent 7900 ICP-MS equipped with a 193 nm laser, housed at the Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Land and Resources of China, Changchun, China. The zircon 91,500 was used as an external standard for age calibration and the NIST SRM 610 silicate glass was applied for instrument optimization. The beam diameter was 32 μm during the analyses. Other instrument parameters and detailed procedures were described by Yuan et al. [6]. Recommended values of U-Th-Pb isotope ratios for zircon standard 91,500 were referred to Wiedenbeck et al. [7] and common Pb was corrected by applying the methods introduced by Andersen [8]. Weighted averages and intercept ages were calculated using the program Isoplot (Version 4.0, United States Geological Survey, Washington, DC, USA). Errors on individual analyses by LA-ICP-MS are quoted at the 2σ level, while errors on the average weighted ages are 2σ level.

3.2.2. Whole-Rock Geochemical Analyses

Five samples (ore-forming rocks) were selected for major and trace element analyses. After the removal of altered surfaces, fresh whole-rock samples were crushed to 200 meshes in an agate mill. Major oxides were determined by using an inductively coupled plasma–optical emission spectroscopy (ICP-OES) system with high-dispersion echelle optics at the China University of Geosciences, Beijing. Loss on ignition was determined by placing 100 mg of sample in a furnace at 980 °C for several hours, cooling the sample in a desiccator and then reweighing the sample. Trace element analyses were performed using an Agilent-7500a inductively coupled plasma-mass spectrometer (ICP-MS) at the China University of Geosciences, Beijing. The rock reference materials AGV-2 (USGS) and GSR-3 (National Geological Standard Reference Materials of China) were used to monitor analytic accuracy and precision. Precision and accuracy are better than 5% for major elements and 10% for trace elements shown from repeated analyses.

4. Analytical Results

4.1. Zircon U-Pb Geochronology

Most of the zircons from the aegirine nepheline syenite (SMN1) are transparent, euhedral and colorless, with length/width ratios of more than 2:1. Typical oscillatory zoning of magmatic crystallization is common in most of the zircon grains under CL (Figure 4). In addition to their relatively high Th/U ratios (0.5–1.0), a magmatic origin is indicated [9,10]. Thirteen zircon U-Pb analyses are summarized in Table 1 and have yielded concordant 206Pb/238U ages of 233 to 222 Ma, with a weighted mean 206Pb/238U age of 229.5 ± 2.2 Ma (MSWD = 0.54; Figure 4).

4.2. Major and Trace Element Geochemistry

The whole-rock major and trace element data from the Saima syenites are presented in Table 2 and Table 3. The aegirine nepheline syenites have variable SiO2 contents of 55.86–80.94 wt. % (concentrating in the range of 55.86–63.80 wt. %) and contain lower TiO2 of 0.36–0.64 wt. %, P2O5 of 0.04–0.11 wt. % and Al2O3 of more than 15 wt. % in most of the samples. They are characterized by relatively high total (K2O + Na2O) values of 9.72–15.51 wt. %, K2O/Na2O ratios of 2.42–3.64 wt. % and Rittmann indexes (σ = [ω(K2O + Na2O)]2/[ω(SiO2 − 43)]) of 6.84–17.10 wt. %, belonging to the high-K peralkaline, metaluminous syenitoid. These rock samples plot into fields of syenite or nepheline syenite in the TAS and R1-R2 diagrams (Figure 5a,b), into field of calc-alkaline series in the FMA diagram (Figure 5c) and into field of metaluminous rocks in the (Fe + Mg + Ti) − [Al − (Na + K + 2Ca)] and A/CNK-A/NK diagrams (Figure 5d,e).
In the primary mantle (PM)-normalized trace element diagram (Figure 6a), the aegirine nepheline syenites are enriched in LILEs (e.g., Cs, Rb and Ba) and depleted in HFSEs (e.g., Nb, Zr, Ti), suggesting that the origin of associated parent magmas is related to the enriched mantle. In addition, these samples have relatively high Nb contents of 34.79–106.59 ppm and are potentially able to provide ore-forming materials for the Nb mineralization. Moreover, the transitional elements show an obvious W-shaped distribution pattern, which are consistent with those from the mantle-derived granite and mafic intrusions formed under continental-rift setting [14].
The aegirine nepheline syenites have variable REE contents varying from 0.34 to 946.00 ppm, with high LREE/HREE ratios of 7.20–18.48 (Table 3). In the chondrite-normalized REE diagram (Figure 6b), these syenites are enriched in LREEs and depleted in HREEs, with high (La/Yb)N ratios of 7.56–39.58, Nb/Ta ratios of 24.56–40.04 and low (Rb/La)N ratios of 0.31–1.14. All of the samples have insignificant negative Sr and Eu anomalies (Eu/Eu* = 0.94–1.00). Considering that the depletions of Sr and Eu were caused by the crystallization of plagioclase or residue in the source [5,15,16,17,18], it is suggested that the plagioclase is absent in the magmatic source of aegirine nepheline syenites. Additionally, the relatively enriched LREEs indicate the presence of garnet as residual mineral in the source [19,20,21,22,23,24].

5. Discussion

5.1. Timing of Nb Mineralization

Based on the Mesozoic diagenetic and metallogenic ages obtained from previous studies in the NE China, three large-scale mineralization events have been identified [29,30,31,32,33]. Chen and Liu et al. pointed out that the Jia–Meng Continental Block collided with the North China Craton along the Xra Moron–Changchun–Yanji Suture Zone, resulted in the intracontinental crustal shortening and thickening and the formation of crustal-derived granitoids and related Cu–Mo–REE mineralization during 255–190 Ma. During 200–130 Ma, a series of EW-, NE-trending regional faults and their secondary faults were developed and reactivated due to the subduction of the Palaeo-Pacific Plate beneath the Eurasian Continent. These faults have provided channels for the ascent of magmas and ore-forming materials, leading to the most intensive mineralization in NE China. North China and Siberian plates collided during 150–120 Ma, resulting in the crustal thickening and the generation of intermediate to felsic magmas and ore-forming fluids. At the same time, the subduction of Pacific oceanic plate entered the peak period at about 140 Ma. The regional tectonic framework in eastern China was then evolved into the coastal western Pacific tectonic domain, leading to the development of the coastal Pacific metallogenic system. These above three large-scale magmatic-mineralized events occurred in NE China, corresponding to the initial subduction and subduction peak of the Palaeo-Pacific Plate, as well as the closure of the Paleo-Asian Ocean Plate, respectively. This reflects that the Mesozoic mineralization events in NE China are associated with the conjunction of multiple plates.
In terms of the Late Triassic intrusive rocks in the eastern Liaoning Province, they were formed under an intracontinental orogenic setting with thickened continental crust. During the earliest Late Triassic, the Liaodong Peninsula was in the retention stage of uplifted mantle, causing the emplacement of massive ultramafic-mafic complex and diorite-quartz diorite-tonalite association along the large-scale lateral ductile shear zone. With the development of intracontinental orogenesis, abundant calc-alkaline granitic rocks originated from the remelting of thickened continental crust emplaced in the Liaodong Peninsula. While, post-orogenic collapse occurred after intracontinental orogeny in the latest Triassic [34,35,36], crustal thinning and the upwelling of mantle-derived magmas resulted in the formation of A-type granites and alkaline complex represented by Saima syenites, which marked the end of the Indosinian magmatism and orogenic cycle.
Sixteen zircon grains with typical magmatic origin from Saima syenite have yielded a weighted mean 206Pb/238U age of 229.5 ± 2.2 Ma (Figure 4), indicating that the ore-related aegirine nepheline syenite emplaced in the Late Triassic. In other words, the metallogenic age of Saima Nb deposit is the Late Triassic. The Nb mineralization at Saima was the product of latest Triassic large-scale mineralization in NE China [31].

5.2. Implications for Tectonic Setting

Recently, it is widely acknowledged that the distribution of REE deposits and their ore-forming rocks were controlled by regional faults in the margins of plates and tectonic conjunctions. This type of REE deposit was genetically related to the magmatism, which shows that the distribution of Nb and Ta metallogenic belt was spatially consistent with the occurrence of magmatic rocks in Liaoning Province [1,37,38,39]. With the deepening of the research on the alkaline rocks, a series of accurate data have been acquired, indicating that the alkali-rich igneous rocks are generally derived from the deep source. These alkaline rocks involve the messages of deep geodynamic processes in the shallow crust, which could reflect the compositions and geodynamic settings of deep earth, the superstructure of the crust and physico-chemical conditions, as well as the concentrations of rare metals in melts. Alkalic complex was known as the product of stable continental rift magmatism and deep fault movements and this property could bring important information about the composition, evolution, tectonic setting and physico-chemistry of deep earth [40,41].
Previous studies have shown that the abnormal geochemical behaviors of Nb and Ta and the ranges of Nb/Ta values during magmatic-hydrothermal processes can reflect the genesis and origin of magmas. The Nb/Ta values from the C1 type chondrite, primitive mantle (PM), depleted mantle (DM) and continental crust are 17.3–17.6, 17.5, 15.5 and 10–14, respectively. Igneous rocks distributed along the deep fault or rift zone show strong enrichments of Nb and Ta, with remarkable high Nb/Ta values than those of primitive mantle [42,43,44,45,46]. The ore-forming syenites in the Saima deposit have obviously higher Nb/Ta values of 24.56–40.04 than those of primitive mantle, which further demonstrated that the Saima syenites were derived from the deep mantle in an extensional environment. Moreover, the syenite samples plot in the field of crust-mantle mixed source in the La/Yb-Eu diagram (Figure 5f). In addition, the Saima syenites show enrichments in Sr and Nd and depletion in Hf, revealing that the asthenospheric mantle had contributed to the generation of ore-related alkaline magmas with Nb and Ta enrichments and high Nb/Ta values. All of the rock samples obtained from the Saima deposit plot in the fields of within-plate, post-collision and rift- granitoids in the tectonic environment discriminant diagrams (Figure 6c,d). The above geochemical characteristics are consistent with those of ore-forming rocks from the same type of deposits and we thus infer that the aegirine nepheline syenite is the ore-forming rock of Saima Nb deposit formed under post-collisional rift setting. The basic characteristics of the deposit are basically consistent with those of typical alkaline-type rare earth deposits, for example, Strange Lake Nb deposit (Canada), Ghurayyah Nb deposit (Saudi Arabia), Khaldzan Buregte (Mongolia) and so on [47,48].
As discussed above, the formation of ore-related aegirine nepheline syenite in the Saima Nb deposit is mainly attributed to crust-mantle mixing. The mineralized processes are summarized as follows. The crust relaxed and thinned after the termination of intracontinental orogeny in the Late Indosinian, causing the upwelling of mantle-derived magmas along the weak zone of a fault system and rising abundant ore-forming materials from deep mantle. The low-degree melting of mantle had resulted in the enrichment of incompatible elements (e.g., LILEs and REEs) and volatile components for the Saima deposit. The aegirine nepheline syenites are enriched in high field-strength elements (particularly for Nb, Ta, Zr and Hf) and LREEs that were higher than those of background values of crust [49,50,51,52], which provide preferable conditions for the formation of Nb mineralization.

6. Conclusions

(1) The Nb orebodies mainly occurred in grey-brown to grass-green aegirine nepheline syenite in the Saima deposit, with fergusonite and brocenite as the dominant ore minerals, which are consistent with the typical alkaline-type REE deposit in China.
(2) In situ LA-ICP-MS zircon U-Pb dating indicates that the aegirine nepheline syenite was emplaced in Late Triassic (229.5 ± 2.2 Ma), which are spatially, temporally and genetically related to Nb mineralization.
(3) The medium-coarse grained aegirine nepheline syenites are high-K peralkaline, metaluminous syenitoid, with relatively high Nb/Ta ratios.
(4) The Saima Nb deposit was formed under the post-collision continental-rift setting, which is consistent with the tectonic regime of post-collision between the North China Craton and Paleo-Asian oceanic plate during the Indosinian. Intensive magmatic and metallogenic events caused by partial melting of lithospheric mantle occurred under the post-collisional rifting, resulting in the development of large-scale Cu–Mo mineralization and rare earth deposits in the eastern of Liaoning Province.

Author Contributions

Conceptualization, Z.-W.B.; Data curation, S.Z., Q.-Q.S., Q.Y. and Z.-G.W.; Methodology, Y.-C.G. and Q.-S.S.; Software, L.S., D.Z. and T.W.; Writing—original draft, Y.-S.R.; Writing—review & editing, N.J.

Funding

This research was funded by the China Geological Survey Project, grant No. DD20160131.

Acknowledgments

We thank the geologists from the Shenyang Geological Survey of CGS with their assistance in the field work for the Saima Nb deposit.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 09 00080 g001 550
Figure 1. Geotectonic location map (a) and Geological sketch map (b) of Saima deposit in Fengcheng, Liaoning Province (modified from [5]).
Figure 1. Geotectonic location map (a) and Geological sketch map (b) of Saima deposit in Fengcheng, Liaoning Province (modified from [5]).
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Minerals 09 00080 g002 550
Figure 2. TCG10-3 trench exploration map of the Saima deposit in Fengcheng, Liaoning Province.
Figure 2. TCG10-3 trench exploration map of the Saima deposit in Fengcheng, Liaoning Province.
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Minerals 09 00080 g003 550
Figure 3. Representative outcrop-pictures and photomicrographs of the ore-forming rocks in Saima niobium deposit. (a) Brown aegirine nepheline syenite; (b) Grass-green aegirine–nepheline syenite(SMN1 is the sample number.); (c) Medium-coarse grained nepheline syenite (PPL); (d) Medium-coarse grained nepheline syenite (CPL); (e) Medium-coarse grained aegirine nepheline syenite (PPL); (f) Medium-coarse grained aegirine nepheline syenite (CPL). Mineral abbreviations: Afs, alkalifeldspar; Arf, arfvedsonite; Bt, biotite; Kfs, K-feldspar; Ne, nepheline; Or, orthoclase.
Figure 3. Representative outcrop-pictures and photomicrographs of the ore-forming rocks in Saima niobium deposit. (a) Brown aegirine nepheline syenite; (b) Grass-green aegirine–nepheline syenite(SMN1 is the sample number.); (c) Medium-coarse grained nepheline syenite (PPL); (d) Medium-coarse grained nepheline syenite (CPL); (e) Medium-coarse grained aegirine nepheline syenite (PPL); (f) Medium-coarse grained aegirine nepheline syenite (CPL). Mineral abbreviations: Afs, alkalifeldspar; Arf, arfvedsonite; Bt, biotite; Kfs, K-feldspar; Ne, nepheline; Or, orthoclase.
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Figure 4. LA-ICP-MS zircon U-Pb concordia diagrams (a) and CL images (b) for the syenite in the Saima deposit.
Figure 4. LA-ICP-MS zircon U-Pb concordia diagrams (a) and CL images (b) for the syenite in the Saima deposit.
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Figure 5. Geochemical classification diagrams for the syenites in the Saima deposit. (a) TAS diagram. (b) R2 vs. R1 diagram. (c) FAM diagram. (d) A/NK vs. A/CNK diagram. (e) [Al − (Na + K + 2Ca)] vs. (Fe + Mg + Ti) diagram. (f) La/Yb vs. Eu diagram (after Le Maître 1989; after Middlemost, 1994; after Irvine, 1971) [11,12,13].
Figure 5. Geochemical classification diagrams for the syenites in the Saima deposit. (a) TAS diagram. (b) R2 vs. R1 diagram. (c) FAM diagram. (d) A/NK vs. A/CNK diagram. (e) [Al − (Na + K + 2Ca)] vs. (Fe + Mg + Ti) diagram. (f) La/Yb vs. Eu diagram (after Le Maître 1989; after Middlemost, 1994; after Irvine, 1971) [11,12,13].
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Figure 6. Geochemical classification diagrams for the syenites in the Saima deposit. (a) Primitive mantle-normalized trace-element diagram (normalized data from Sun and Mcdonough,1989); (b) Chondrite-normalized rare-earth element (REE) patterns (normalized data from Boynton, 1984); (c,d) Structural discriminant diagram (after Defant and Drummond, 1990; modified from Pearce 1982) [25,26,27,28].
Figure 6. Geochemical classification diagrams for the syenites in the Saima deposit. (a) Primitive mantle-normalized trace-element diagram (normalized data from Sun and Mcdonough,1989); (b) Chondrite-normalized rare-earth element (REE) patterns (normalized data from Boynton, 1984); (c,d) Structural discriminant diagram (after Defant and Drummond, 1990; modified from Pearce 1982) [25,26,27,28].
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Table
Table 1. LA-ICP-MS zircon U-Pb analysis results for the syenite in the Saima deposit.
Table 1. LA-ICP-MS zircon U-Pb analysis results for the syenite in the Saima deposit.
Sample No.Isotopic RatiosAge (Ma)
206Pb/238U1σ207Pb/235U1σ207Pb/206Pb1σ208Pb/232Th1σ232Th/238U206Pb/238U1σ207Pb/235U1σ208Pb/232Th1σ
10.03650.00060.26950.01060.05350.00230.01180.00020.8691231424282385
20.03640.00050.25890.00510.05150.00130.01220.00020.3079231323442463
30.03640.00060.25480.01170.05080.00250.01140.00020.8899230423092295
40.03560.00080.24890.01850.05070.00390.01310.00031.22282265226152635
50.03690.00110.26480.03030.05210.00610.01080.00040.99872337239242189
60.03650.00070.25440.01600.05060.00330.01120.00040.71792315230132269
70.03610.00160.24700.04380.04960.00900.01300.00120.5357229102243626223
80.03510.00070.25380.01540.05250.00330.01090.00040.55542224230122197
90.03670.00080.26060.01730.05160.00360.01160.00031.75062325235142325
100.03630.00110.26150.02840.05220.00590.00970.00050.626523072362319510
110.03590.00060.25510.00780.05160.00180.01120.00021.1001227323162263
120.03640.00050.25430.00720.05070.00160.01150.00011.5393230323062323
130.03660.00060.25580.00720.05060.00160.01240.00014.8276232323162492
Table
Table 2. Whole-rock major oxides (wt. %) of syenites in the Saima deposit.
Table 2. Whole-rock major oxides (wt. %) of syenites in the Saima deposit.
Sample No.SiO2Al2O3TFe2O3MgOCaONa2OK2OMnOTiO2P2O5LOITotal
SMH1-163.8015.253.500.511.592.579.360.090.360.102.89100.02
SMH1-280.941.162.640.031.262.537.180.070.460.043.69100.00
SMH1-357.1619.113.720.451.574.5310.980.080.410.081.9099.99
SMH1-457.3818.113.680.531.954.0710.250.090.640.113.1899.98
SMH1-555.8618.813.960.702.114.2510.580.100.620.112.91100.00
Table
Table 3. Whole-rock trace and rare-earth elements (ppm) of syenites in the Saima deposit.
Table 3. Whole-rock trace and rare-earth elements (ppm) of syenites in the Saima deposit.
Sample No.LiTiScVCrCoNiCuZnGaRbSrYMnZrNbHfCsBa
SMH1-169.942608.202.3064.8715.267.070.9230.9485.4129.11312.202846.0073.54804.80410.8037.899.062.903366.00
SMH1-261.384044.601.4071.0312.844.790.1228.8373.2624.17214.201171.2077.84706.20888.20106.5920.302.932528.00
SMH1-340.372552.401.8861.5614.454.460.9125.4298.4830.28290.202750.0049.60676.40380.4034.797.842.502708.00
SMH1-455.554221.002.4560.9115.325.142.4529.0198.5130.49287.602900.00112.72766.80629.8069.3914.052.952912.00
SMH1-551.153943.802.4759.1113.105.9530.5126.30103.1432.06292.802742.00154.16774.80532.6074.7411.892.932396.00
Sample No.LaCePrNdSmEuGdTbDyHoErTmYbLuTaPbThU
SMH1-1227.60446.0048.36159.8026.627.3819.042.5613.272.486.650.834.850.561.4160.88127.1018.02
SMH1-291.50186.0226.8095.3619.876.0215.952.7316.603.419.951.378.160.942.6648.80124.4238.53
SMH1-3176.90320.6033.80110.9019.395.5314.371.959.951.804.610.553.010.341.4269.5389.8513.03
SMH1-4340.00667.6077.48233.4038.3410.5927.823.8119.913.709.781.226.980.812.6079.18189.3232.25
SMH1-5466.00946.00108.26331.6055.3815.1440.245.5629.085.3513.871.679.080.992.3556.45275.5041.75

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Ju, N.; Ren, Y.-S.; Zhang, S.; Bi, Z.-W.; Shi, L.; Zhang, D.; Shang, Q.-Q.; Yang, Q.; Wang, Z.-G.; Gu, Y.-C.; et al. Metallogenic Epoch and Tectonic Setting of Saima Niobium Deposit in Fengcheng, Liaoning Province, NE China. Minerals 2019, 9, 80. https://doi.org/10.3390/min9020080

AMA Style

Ju N, Ren Y-S, Zhang S, Bi Z-W, Shi L, Zhang D, Shang Q-Q, Yang Q, Wang Z-G, Gu Y-C, et al. Metallogenic Epoch and Tectonic Setting of Saima Niobium Deposit in Fengcheng, Liaoning Province, NE China. Minerals. 2019; 9(2):80. https://doi.org/10.3390/min9020080

Chicago/Turabian Style

Ju, Nan, Yun-Sheng Ren, Sen Zhang, Zhong-Wei Bi, Lei Shi, Di Zhang, Qing-Qing Shang, Qun Yang, Zhi-Gao Wang, Yu-Chao Gu, and et al. 2019. "Metallogenic Epoch and Tectonic Setting of Saima Niobium Deposit in Fengcheng, Liaoning Province, NE China" Minerals 9, no. 2: 80. https://doi.org/10.3390/min9020080

APA Style

Ju, N., Ren, Y. -S., Zhang, S., Bi, Z. -W., Shi, L., Zhang, D., Shang, Q. -Q., Yang, Q., Wang, Z. -G., Gu, Y. -C., Sun, Q. -S., & Wu, T. (2019). Metallogenic Epoch and Tectonic Setting of Saima Niobium Deposit in Fengcheng, Liaoning Province, NE China. Minerals, 9(2), 80. https://doi.org/10.3390/min9020080

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