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Article

Identification and Geological Significance of Early Jurassic Adakitic Volcanic Rocks in Xintaimen Area, Western Liaoning

by
Zhi-Wei Song
1,
Chang-Qing Zheng
1,2,*,
Chen-Yue Liang
1,2,
Bo Lin
1,
Xue-Chun Xu
1,
Quan-Bo Wen
1,
Ying-Li Zhao
1,
Cheng-Gang Cao
3 and
Zhi-Xin Wang
4
1
College of Earth Sciences, Jilin University, Changchun 130061, China
2
Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Land and Resources, Jilin University, Changchun 130061, China
3
Qinghai Bureau of Environmental Geology Exploration, Xining 810008, China
4
Shandong No.3 Exploration Institute of Geology and Mineral Resources, Yantai 264000, China
*
Author to whom correspondence should be addressed.
Minerals 2021, 11(3), 331; https://doi.org/10.3390/min11030331
Submission received: 4 February 2021 / Revised: 12 March 2021 / Accepted: 18 March 2021 / Published: 23 March 2021
(This article belongs to the Special Issue Isotope Dating and Geochemistry of Granite)
Browse Figures
Versions Notes

Abstract

:
The Western Liaoning area, where a large number of Jurassic-Cretaceous volcanic rocks are exposed, is one of the typical areas for studying the Mesozoic Paleo-Pacific and Mongolia-Okhotsk subduction process, and lithospheric destruction of North China Craton. The identification and investigation of Early Jurassic adakitic volcanic rocks in the Xintaimen area of Western Liaoning is of particular significance for exploring the volcanic magma source and its composition evolution, tracking the crust-mantle interaction, and revealing the craton destruction and the subduction of oceanic plates. Detailed petrography, zircon U–Pb dating, geochemistry, and zircon Hf isotope studies indicate that the Early Jurassic intermediate-acidic volcanic rocks are mainly composed of trachydacites and a few rhyolites with the formation ages of 178.6–181.9 Ma. Geochemical characteristics show that they have a high content of SiO2, MgO, Al2O3, and total-alkali, typical of the high-K calc-alkaline series. They also show enrichment of light rare earth elements (LREEs) and large ion lithophile elements (LILEs), depletion of heavy rare earth elements (HREEs) and high field strength elements (HFSEs), and have a high content of Sr and low content of Y and Yb, suggesting that they were derived from the partial melting of the lower crust. The εHf(t) values of dated zircons and two-stage model ages (TDM2) vary from −11.6 to −7.4 and from 1692 to 1958 Ma, respectively. During the Early Jurassic, the study area was under long-range tectonic effects with the closure of the Mongolia-Okhotsk Ocean and the subduction of the Paleo-Pacific plate, which caused the basaltic magma to invade the lower crust of the North China Craton. The mantle-derived magma was separated and crystallized while heating the Proterozoic lower crust, and part of the thickened crust melted to form these intermediate-acidic adakitic volcanic rocks.

1. Introduction

Adakite has attracted much attention due to its unique magma source, geodynamic significance, and close relationship with metal deposits. The term “adakite” originally refers to a set of intermediate-acidic igneous rocks formed by slab melting in the subduction environment, with geochemical characteristics of MgO ≤ 3 wt.%, SiO2 ≥ 56 wt.%, Al2O3 ≥ 15 wt.%, La/Yb ≥ 20, Sr/Y ≥ 40, and/or low Y ≤ 18 ppm [1,2,3,4]. However, some intermediate-acidic igneous rocks with the geochemical characteristics of adakite are not necessarily developed in an island arc environment or by the melting of subducted slabs [5,6,7,8,9,10,11]. These rocks are collectively referred to as adakitic rocks. In this study, a set of intermediate-acidic adakitic volcanic rocks with high-K calc-alkaline series affinity were identified in the Western Liaoning area, which is located on the northern margin of the North China Craton (NCC; Figure 1).
As one of the oldest cratons in the world, the NCC has a long history of ~3.8 billion years, which preserves a relatively complete tectonic evolution that contains metamorphic basement from Archean to Paleoproterozoic and Phanerozoic caprock development (Figure 1) [12,13,14,15,16,17,18,19]. The Western Liaoning is located in the northern margin of the NCC and the eastern part of the Yanshan tectonic belt which developed a large number of Mesozoic volcanic-sedimentary basins with lots of lacustrine paleontological fossils. Therefore, Western Liaoning is one of the classic areas to study the Mesozoic tectonic-magma and biological evolution in the NCC (Figure 1 and Figure 2) [6,18,20,21,22,23,24,25,26].
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Figure 1. Simplified map showing the tectonic subdivisions of the North China Craton and the distribution of the basement rocks (modified after Zhao et al. [13]; NCC for North China Craton, SCC for South China Craton).
Figure 1. Simplified map showing the tectonic subdivisions of the North China Craton and the distribution of the basement rocks (modified after Zhao et al. [13]; NCC for North China Craton, SCC for South China Craton).
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Since the Mesozoic, the Western Liaoning region was affected by the superimposition of the NE trending Paleo-Pacific plate tectonic domain, Mongolia-Okhotsk tectonic domain and the nearly EW trending Central Asian Orogenic Belt (CAOB). In complex tectonic regimes, the wide development of Mesozoic volcanic rocks began in the Early Jurassic and ended in the late Early Cretaceous. Geochronology of the Mesozoic volcanic events in the Western Liaoning region have been studied in detail by predecessors, which can be divided into four phases: Early Jurassic (Nandaling or Xinglonggou Period), Late Jurassic (Tiaojishan or Lanqi Period), Early Cretaceous (Zhangjiakou or Yixian Period), and Late Cretaceous (Daxingzhuang Period) [6,24,27,28,29,30,31,32,33,34,35,36,37]. However, most of the geochronological and biological studies focused on the Late Jurassic-Early Cretaceous magmatic events, and most scholars believed that the Late Jurassic magmatic rocks may be the result of the Paleo-Pacific subduction [6,20,21] or the combined influence of the subduction and closure of the Mongolia-Okhotsk Ocean [38,39,40]. The widely distributed Early Cretaceous magmatic rocks were formed under a strong extensional background, which was related to the subduction of the Paleo-Pacific plate [20,21,25,26,40,41]. However, the distribution and tectonic setting of the Early Jurassic volcanic rocks are still controversial [6,36,37,39,42,43].
A wide range of volcanic rocks was exposed in the Xintaimen area, Western Liaoning region, but the only research was mostly focused on the Yanliao biota and Jehol biota which occur in this area [44,45,46,47], and their ages were roughly defined as the middle and late Early Cretaceous. However, detailed fieldwork has found that the large-scale Early Jurassic adakitic volcanic rocks now identified in the Western Liaoning region, previously were rarely reported and were included in the middle and late Early Cretaceous biota divisions. This paper conducts a systematic study on the Early Jurassic volcanic rocks, including petrology, geochemistry, zircon U-Pb chronology, and Lu-Hf isotope analysis, and then discusses its magma origin, petrogenesis, and crust-mantle interaction, all of which provide a key position and important window for understanding the subduction process of the Paleo-Pacific plate and the superposition, conversion, and transformation of different tectonic regimes (Figure 1) [48,49,50,51].
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Figure 2. Geological map of Western Liaoning province (a); modified after Lin [52]) and distribution of Early Jurassic volcanic rocks with sampling locations (b). Note: The rectangle (b) in Figure 2a shows the location of Figure 2b. Figure 2a shows a traditional understanding of the basin distribution, Figure 2b shows the volcanic rocks based on new-age data. Therefore, the area displayed as green in Figure 2a becomes blue in Figure 2b.
Figure 2. Geological map of Western Liaoning province (a); modified after Lin [52]) and distribution of Early Jurassic volcanic rocks with sampling locations (b). Note: The rectangle (b) in Figure 2a shows the location of Figure 2b. Figure 2a shows a traditional understanding of the basin distribution, Figure 2b shows the volcanic rocks based on new-age data. Therefore, the area displayed as green in Figure 2a becomes blue in Figure 2b.
Minerals 11 00331 g002

2. Geological Setting

The northern boundary of NCC is the Central Asian Orogenic Belt, adjacent to the Siberian Craton, and its eastern edge is connected with the Pacific plate, and its southern boundary is the Qinling-Dabie-Sulu ultrahigh-pressure belt, adjacent to the South China Craton (Figure 1). From Late Paleozoic to Mesozoic, the Western Liaoning region in the east of NCC has experienced a complex superimposition of the subduction and closure of the Paleo-Asian Ocean, the Paleo-Pacific tectonic regime, and the Mongolia-Okhotsk tectonic regime, which resulted in the thinning of the lithosphere and the strong tectonic-magmatic-metallogenic-basin-forming activities. The Mesozoic era is considered to be the main period of destruction of the NCC, which is the active period of strong Yanshan tectonic movement and magmatic activities such as lithospheric thinning and destruction, plate subduction, intracontinental orogeny, regional uplifting, and extension [18,22,41,53,54]. Therefore, Mesozoic volcanic rocks are closely related to such geological issues as the Mesozoic tectonic transformation in eastern China, crustal delamination and thinning in eastern NCC, and the biota expansion, which directly affect geologists’ understanding of the ages and background of different geological events. [6,41,55].
Volcanic rocks are well developed in Western Liaoning, mainly distributed in the Mesozoic Jinlingsi-Yangshan volcanic belt and Fuxin-Yixian basin belt [33,34,56]. The volcanic activities began in the Late Triassic and reached the peak in the Early Cretaceous. According to the residual strata of the present basin in the study area, the volcanic-sedimentary basins widely developed in Western Liaoning can be divided into Jurassic basin and Cretaceous basins, among which the Jurassic basin is the Jinlingsi-Yangshan basin, and the Cretaceous basin is more extensive, such as Xiaodeyingzi basin, Xintaimen basin, Sierbao-Baita basin, and so on (Figure 2a). The main strata developed are volcanic rocks of the Guajishan Formation and Yixian Formation which are distributed in a NE direction. With further research, it is gradually discovered that a large number of Jurassic volcanic-sedimentary strata develop in the original thought Cretaceous basin. The Xintaimen basin is located in the northwestern part of the Yangjiazhangzi magmatic-metallogenic belt (Figure 2a,b). The first 40Ar/39Ar dating results of the andesite and basaltic andesite exposed in the basin were from the late Early Cretaceous to the early Late Cretaceous (110.9–92.8 Ma) [46]. A large number of salamander fossils belonging to the Jehol biota were found in the lacustrine purple argillaceous siltstone interbedded with gray-green andesite [44,50], and the basin was classified as the Early Cretaceous basin. This study now reports that large-scale Early Jurassic volcanic rocks are distributed in the Xintaimen basin in the NNE direction, which rests angular discordant on the limestone of Early and Middle Proterozoic Wumishan Formation and the limestone strata of Early Paleozoic. The rock assemblages of the volcanic rocks are mainly intermediate-acidic volcanic rocks which are composed of trachyandesite, trachyte, trachydacite, and a small amount of rhyolite. The detailed determination of the analyzed volcanic rocks is of great significance for establishing the chronological framework, petrogenesis, and tectonic setting of Mesozoic volcanic rocks in the Western Liaoning region.

3. Sample Descriptions

The typical volcanic rocks were selected for systematic analysis, and the main samples were classified into two groups. Trachydacites with a light gray or light purple gray colors are the most widely distributed in the basin. They have a porphyritic texture, a massive structure, and a fluidal structure that can be seen locally. Phenocrysts account for 5–30% (Figure 3a,b), are mainly composed of plagioclase, hornblende, and biotite. The plagioclase is euhedral or subhedral granular with a polysynthetic twin. Some plagioclases have the characteristics of multiple crystallization, and the centers of some plagioclases have been altered. The hornblende is euhedral granular with black, some of which are directional. The matrix is a mikropoikilitic texture composed of irregular quartz inlaid with fine feldspar microcrystals (Figure 3c; YX-06).
Rhyolites are less exposed and mainly distributed in the trachyandesite interlayer. The weathered surface of the rocks is earth yellow, and the fresh surface is grayish-white or light yellow. It has a porphyritic and massive structure, and the phenocryst content is about 15–25%. The porphyritic minerals are mainly composed of plagioclase, hornblende, quartz, and a small amount of biotite. The plagioclase is euhedral granular with a slight alteration, and part of the plagioclase presents a polysynthetic twin. The hornblende is euhedral granular with dark green. Quartz is xenomorphic granular and biotite is a brown flake. The matrix is mainly a fluidal structure composed of quartz and feldspar and other microcrystalline minerals (Figure 3d; YX-07).

4. Analytical Methods

4.1. Zircon U-Pb Dating

The trachydacite (YX-06) and rhyolite (YX-07) were selected for zircon U–Pb isotopic dating. The sorting of zircon single mineral was completed in Langfang Regional Geological Survey, Hebei Province, China. The sample target was prepared and handmade in Beijing GeoAnaly/i/Co., Ltd., Beijing, China. LA–ICP–MS U–Pb zircon dating was carried out at the Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Natural Resources, Jilin University, Changchun, Jilin, China, using an ArF excimer laser system (GeoLas Pro, 193 nm wavelength) and a quadrupole ICP–MS (Agilent 7500a, Santa Clara, CA, USA). Some zircons have multiple zoning, however, we choose potential target sites carefully and ensured the reliability of our data which avoided a single analysis spot crossing multiple zones. Details of the analytical methods are given by Liang et al. [57]. The software Glitter was used to calculate the isotope ratio and element content. The data calculation and image rendering were processed using the ISOPLOT program (Version 3.23) [58]. Common Pb was corrected for following Andersen [59]. Uncertainties on individual analyses were reported with 1σ error and weighted mean ages were calculated at 1σ confidence level, representing the 95% confidence interval. The filtering of the U–Pb ages was based on a 10% cut-off of the calculated discordance (%U–Pb disc = [1 − (206Pb/238U age/207Pb/235U age)] × 100). The 206Pb/207Pb age for zircons with ages greater than 1000 Ma was used, instead, for grains younger than 1000 Ma, the 206Pb/238U age was used as the best age independence of the imprecise measurement of 207Pb in young grains.

4.2. Major- and Trace-Element Analyses

The pre-processing and analysis of the whole-rock samples were completed in the Test Center of No.1 Bureau of China Metallurgical Geology Bureau, Hebei Province, China. The major elements were analyzed by an X-ray fluorescence spectrometer (XRF, Japan Rigaku), and the testing instrument was a sequential X-ray fluorescence spectrometer (AXIOS Minerals). Trace elements were tested by an inductively coupled plasma mass spectrometer (ICP–MS Agilent 7500ce). Details of the analytical methods are given by Hu et al. [60].

4.3. Zircon Lu-Hf Isotope Analyses

Based on the LA–ICP–MS U–Pb zircon dating, the in situ zircon Hf isotopic analysis of Mesozoic volcanic rocks in the Xintaimeng basin was carried out. The analysis was conducted using a Neptune Plus MC–ICP–MS (Thermo Fisher Scientific, Darmstadt, Germany) in combination with a Geolas 2005 excimer ArF laser ablation system (193 nm) that was hosted at the Solid Isotope Laboratory of Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing, China. The analysis spots were 44 μm in diameter, and each measurement consisted of the 20 s of acquisition of the background signal followed by 50 s of acquisition of the ablation signal. The international standard sample 91,500 of zircon was used as the external standard for the measurement. The laser ablation rate was 8 Hz and the energy was 90 mJ. Offline processing of analysis data (including the selection of samples and blank signals, and isotope mass fractionation correction) was completed by ICPMSDataCal software. Details of the analytical techniques are given by Hu et al. [61].

5. Analytical Results

5.1. Zircon U-Pb Ages

Zircons from trachydacite YX-06 (N: 40°55′25″, E: 120°24′46″) and rhyolite YX-07 (N: 40°56′11″, E: 120°26′50″) are both euhedral-subhedral, with grain sizes ranging from 150–300 μm (Figure 4a,b). The elongation (length to width) ratios of zircons range from 1.5:1 to 2.5:1, suggesting a faster crystallization velocity. The CL image shows that the zircons have a clear internal structure, complete crystal shape, and mostly long columnar form, with a typical oscillatory growth zoning. Most zircons have locally preserved xenocrystic cores, which occur as cores mantled by newly grown zircon (Figure 4a,b). The occurrence of xenocrystic zircon is a common feature of many igneous rocks [62]. In addition, these zircons show continuity between core and rim, having high U contents (ranging from 101 to 6632 ppm) and Th/U ratios mostly between 0.26 and 3.19 (Table 1), indicating magmatic origin.
A total of 25 zircons were analyzed in trachydacite YX-06, all of which were located near the concordia curve (Figure 4c). The weighted mean 206Pb/238U age from the 15 zircon grains is 181.9 ± 3.0 Ma (MSWD = 4.2, n = 15), which represents the timing of crystallization of this sample is late Early Jurassic. Seven zircon grains exhibit Paleoproterozoic ages, with a weighted mean 206Pb/238U age of 2486 ± 31 Ma (MSWD = 3.8, n = 7), indicating inherited or captured zircons. The weighted mean 206Pb/238U age from the two zircon grains is 132.1 ± 2.5 Ma (MSWD = 0.62, n = 3), which may be attributed to the later tectonic thermal events.
A total of 25 zircons tested from rhyolite YX-07 (Figure 4d) gave 206Pb/238U ages of 19 zircons which ranged from 169 to 191 Ma, with a weighted mean 206Pb/238U age of 178.8 ± 1.9 Ma (MSWD = 2.2, n = 19), indicating the crystallization age of late Early Jurassic. The 206Pb/238U ages of the 2 zircons are 198 ± 3 Ma and 2466 ± 18 Ma, respectively, which may be the ages of the inherited zircons. The weighted mean 206Pb/238U age from the two zircon grains is 121.3 ± 4.7 Ma (MSWD = 0.16, n = 2), indicating the late Early Cretaceous, which may represent the age of late tectonic thermal events. The two discordant ages probably are disturbed by Pb loss (%U–Pb disc > 10, Table 1), so they are inaccurate and are not used during our mapping.

5.2. Geochemical Features

5.2.1. Major Elements

Twelve typical fresh Early Jurassic intermediate-acidic volcanic rocks were selected for geochemical analysis, and the results are shown in Table 2 and Table 3. The SiO2 in volcanic rocks is 60.70~71.45 wt.%, which is a set of intermediate-acidic magmatic rocks. The volcanic rocks contain Mg# [Mg# = 100 Mg2+/(Mg2+ + TFe2+)] values of 16–48, 0.23–0.77 wt.% TiO2, 2.05–6.14 wt.% TFeO, 14.23–16.81 wt.% Al2O3, 0.63–4.21 wt.% CaO, 3.46–6.01 wt.% Na2O, 3.35–5.85 wt.% K2O, 0.79–1.79 Na2O/K2O, and (Na2O + K2O) concentrations of 7.79–11.28 wt.% (Table 2). In the total-alkali vs. silica (TAS) diagram (Figure 5a), they fall into trachyte and rhyolite areas respectively (the normative Quartz more than 20 wt.% in most samples). In the SiO2 vs. K2O diagram (Figure 5b), the samples mainly fall into the area of high-K calc-alkaline series, and a small amount falls into the area of the shoshonite series. They have A/CNK values of 0.99–1.09, indicating they are metaluminous to weakly peraluminous (Figure 5c).
According to the Harker diagram (Figure 6), there is a negative correlation between the major elements and SiO2. These geochemical variations can be attributed to mineral fractional crystallization during magmatic evolution. MgO, TFeO, CaO have an approximately negative correlation with SiO2, which may indicate the fractional crystallization of clinopyroxene and hornblende. The decreases in Al2O3 and Sr concentrations with increasing SiO2 probably relate to the fractionation of plagioclase. In addition, the decrease in TiO2 with increasing SiO2 content can be attributed to fractional crystallization of titaniferous minerals such as rutile, ilmenite, and sphene. In summary, we propose that mineral fractional crystallization during magmatic evolution is responsible for compositional variations in these volcanic rocks.

5.2.2. Trace and Rare Earth Elements

In the primitive mantle normalized trace element spidergrams (Figure 7a), the samples are relatively enriched in large ion lithophile elements (LILEs; e.g., Ba, Rb, K, and Sr), depleted in high field strength elements (HFSEs; e.g., Nb, Ta, Ti, and P), and have obvious geochemical characteristics of positive Pb anomalies. The samples are enriched in LILEs, Pb, and HFSEs (Zr and Hf), in which Ba is more enriched than Rb and Th, and HFSEs (Nb, Ta, and Ti) are relatively depleted, indicating the characteristics of continental crust. The ratios of Sr/Y and Nb/Ta are high, and the contents of LILEs such as Sr (340–865 μg/g, except XY-07), Ba (907–1565 μg/g), U (0.58–1.77 μg/g), and Th (2.92–10.5 μg/g) are high, which are similar to the geochemical characteristics of adakitic volcanic rocks. In the chondrite normalized REE patterns (Figure 7b), the samples are enriched in light rare earth elements (LREEs) and depleted in heavy rare earth elements (HREEs), showing an overall right-leaning curve as a whole, with obvious fractionation of light and heavy rare earth elements ((La/Yb)N = 16.70–38.71), as well as weak negative Eu anomalies (δEu = 0.7–1.04). The Yb content is less than 0.75 μg/g, and the Y content is less than 7.5 μg/g, which may imply that there are residual garnet and other minerals in the source area and the crystallization separation of the plagioclase is not obvious during the original magma evolution. The lower contents of the compatible elements Co (2.83–7.54 μg/g), Ni (2.03–15.4 μg/g), and Cr (5.66–26.5 μg/g) suggest that the magma may have originated from partial melting of crustal materials.

5.3. Zircon Hf Isotopes

On the basis of U–Pb zircon dating, Lu–Hf isotopic analysis of representative zircons was carried out, and the analysis results are shown in Table 4. The results show that the 176Hf/177Hf ratios of the seven zircons with a crystallization age of about 181 Ma in the sample YX-06 range from 0.282222 to 0.282339. The corresponding εHf(t) values range from −16.0 to −11.7, and the two-stage model ages (TDM2) range from 1961 to 2232 Ma, suggesting that the source area may be derived from the ancient lower crust of the Proterozoic (Table 4, Figure 8). It is worth noting that the ~174 Ma zircon have 176Hf/177Hf ratio of 0.282619, εHf(t) value of −2.3, and the two-stage model age (TDM2) of 1363 Ma, indicating that the magma source area may be contributed by depleted mantle material (Table 4, Figure 8). The 176Hf/177Hf ratios of the 13 zircons with a crystallization age of about 178Ma in the sample YX-07 range from 0.282337 to 0.282457. The corresponding εHf(t) values range from −11.6 to −7.4, and the two-stage model ages (TDM2) range from 1692 to 1958 Ma, which also suggests that the magma may be derived from the Proterozoic lower crust (Figure 8).

6. Discussion

6.1. Formation Ages

The Xintaimen basin in Western Liaoning was well-known in recent years because of a large number of the Jehol biota fossils in the lacustrine sediments, such as the Liaoxitriton zhongjiani and associated Eosestheria and Liaoningocladusboii [44,45]. It consists of the Lower Cretaceous Yixian Formation and/or Jiufotang Formation. Further research from Sun et al. conducted 40Ar/39Ar dating of widely developed volcanic rocks, which indicated their likely formation in the late Early Cretaceous or the early Late Cretaceous (93–110 Ma) [46]. However, the latest zircon U–Pb dating results of volcanic rocks in this paper show that the Xintaimen basin also developed a large range of Early Jurassic acidic volcanic rocks, with a formation age of 178.6–181.9 Ma. The rock assemblages are trachyandesite, trachydacite, a small amount of rhyolite and andesitic pyroclastic rocks, which are spatially distributed in the NNE or NS direction.
The Eastern Hebei and Western Liaoning areas on the eastern margin of the NCC were successively affected by the interaction of the Tethyan tectonic domain, the Paleo-Asian Ocean tectonic domain, and the Paleo-Pacific tectonic domain. Massive igneous rocks have been exposed in the Yanshan region located on the northern margin which is characterized by the superposition of multi-stage tectonic-magmatic activities [6,39,43,55,70,71]. The activity of Mesozoic vulcanism can be divided into four periods: Early Jurassic (Nandaling or Xinglonggou Period), Late Jurassic (Tiaojishan or Lanqi Period), Early Cretaceous (Zhangjiakou or Yixian Period), and Late Cretaceous (Daxingzhuang Period) [6,29,35,36,37,39,43,71,72]. Among these, the distribution range of Early Jurassic volcanic rocks is relatively limited and weak inactivity. The volcanic rocks are mainly composed of basalt, basaltic trachyandesite, andesite, trachyandesite, trachyte, and dacite [6,35,36,37,43]. The sporadic intermediate-basic volcanic rocks (174 Ma) from the Nandaling Formation in Xishan, Beijing, the intermediate volcanic rocks (202–177 Ma) from the Xinglonggou Formation in Beipiao, Western Liaoning, and the intermediate volcanic rocks (183–173 Ma) from the Haifanggou Formation in Beipiao, Western Liaoning are all products of volcanic activities in this period [43,55,70,71], which is basically consistent with the dating results of this paper (178.6–181.9 Ma).

6.2. Petrogenesis and Magma Source

The Early Jurassic volcanic rocks in the Western Liaoning are a set of intermediate-acidic rock assemblages, including trachyandesite, trachydacite, and a small amount of rhyolite and basaltic trachyandesite. From the perspective of petrochemical characteristics, Early Jurassic volcanic rocks have adakitic geochemical characteristics, such as high SiO2 (60.94–71.45 wt.%), Al2O3 (≥14.41 wt.%), and Na2O (≥3.46 wt.%), with high Sr content between 395–1022 ppm (except YX-07, YX-08), low Y (5.74–15.68 ppm, <18 ppm), and Yb (0.55–1.58 ppm, <1.9 ppm). The samples are enriched in LREEs and LILEs, depleted in HREEs and HFSEs [2,73], without Eu anomalies (Eu/Eu* = 0.71–1.07), and fall into the adakitic rocks area in (Yb)N-(LA/Yb)N and Y-Sr/Y diagrams (Figure 9a,b). Therefore, this set of Early Jurassic intermediate-acidic volcanic rocks should be adakitic rocks.
The rocks can be produced by the partial melting of the subducting oceanic crust interacting with the overlying mantle peridotite [2,73], by the crystallization differentiation of basaltic magma and crustal contamination [3], by partial melting of basaltic rocks and eclogite in the delamination lower crust [6,74,75], or by partial melting of ancient (thickened) basaltic lower crust [35,36,76,77]. However, the high K2O content, K2O/Na2O and Sr/Y ratios, low HREEs, weak negative Eu anomaly, and inherited zircon with crystalline basement age indicate that the volcanic rocks cannot have been formed in the partial melting of subducted oceanic plate [37,71]. At the same time, the SiO2 content of most samples is higher (>66%), with low MgO, Mg#, Cr, Ni, and other characteristics, which are also different from the partial melting characteristics of the hydrated mantle [2,73]. Lower MgO, Cr, Ni, Sc, Co contents and Mg# values [75,78], combined with the fact that Early Jurassic basalts have not been found in the Xintaimen area, indicate that the initial magma was not the product of crystallization differentiation of basaltic magma, or was not affected by mantle magma contamination, or did not interact with mantle peridotite, which excludes it as the product of partial melting of the delamination lower crust (Figure 10d). Low Ce/Pb (<3.6), Th, and U values indicate that lower crust materials are involved in the source area or magma evolution [79], and their higher Sr/Y ratios may be the characteristics of the inherited source area. In addition, the linear relationship between the major elements and SiO2 content suggests the existence of fractional crystallization during the magmatic evolution [80]. Furthermore, the Lu-Hf isotope results show that the value of εHf(t) ranges from −11.6 to −7.4, and the two-stage model ages (TDM2) range from 1692 to 1958 Ma, indicating that its magma source should be the partial melting of the lower crust of the Proterozoic (Figure 8). Therefore, this set of intermediate-acidic adakitic volcanic rocks originated from partial melting of the Proterozoic basaltic rocks in the lower crust of the NCC, nevertheless mantle-derived magma may also be involved. The partial melting of the lower crust caused by the underplating of basaltic magma is considered to be one of the main mechanisms for the formation of Mesozoic adakitic rocks in North China [5,35,36,76,77]. In the inland areas far from the subduction zone, the underplating event of mantle-derived basaltic magma cannot only thicken the lower crust, but also provide huge heat energy to promote partial melting of the lower crust rock to form adakitic magma [5,81]. Early-Middle Jurassic zircon ages in the lower crustal xenoliths of the Hannuo Dam in North China, indicate that there was a magmatic underplating event during the Early Jurassic–Middle Jurassic [25,55,82]. The underplating basaltic magma is generally considered to be not involved in the melting process or to play a lower role, resulting in the formation of adakitic magma with low Cr, Ni, Co, SC, Mg#, and MgO contents, which is similar to the geochemical characteristics of Early Jurassic intermediate-acidic volcanic rocks in the study area. The underplating basaltic magma may also have crust-mantle interaction with the lower crustal magma, forming a small amount of basaltic magma, and leading to the abnormal value of εHf(t) [52]. Therefore, during the process of basaltic magma in the NCC underplating the basic lower crust in the Early Jurassic, the mantle-derived magma underwent fractional crystallization while heating the overlying ancient (Proterozoic) lower crust, and part of the thickened crust melted to form adakitic magma. Because the Ni, Cr concentrations and Mg# values have not increased significantly, adakitic magma may not be mixed with differentiated mantle-derived magma, or only mixed with a small amount of differentiated mantle-derived magma. Then, the acidic magma chamber was formed by fractional crystallization of mafic minerals, and finally, it rose rapidly and was expelled from the surface to form intermediate-acidic volcanic rocks with high Sr/Y and low REE.

6.3. Geological Implication

Western Liaoning is located in the superposition of the Tethys tectonic domain, the Paleo-Asian Ocean tectonic domain and the Paleo-Pacific tectonic domain [84]. It is one of the important regions for studying intracontinental orogeny, Yanshan movement, lithospheric thinning, and destruction of NCC [6,18,30,85,86]. The Yanshan region experienced large-scale tectonic deformation and magmatic activities, and developed a large-scale NE-NNE-trending fault basin. During the Mesozoic, it experienced the transition from convergence regime dominated by the Paleo-Asian Ocean tectonic domain to the subduction regime dominated by the Paleo-Pacific tectonic domain [29,51,72,77,87,88,89], which led to strong tectonism, magmatism, and mineralization [40,41,90].
The Early Jurassic volcanic rocks are sporadically distributed in Eastern Hebei and Western Liaoning, including the Nandaling Formation in Xishan, Beijing, Xinglonggou Formation in Chengde, Hebei and Western Liaoning, and Haifanggou Formation in Western Liaoning [6,35,36,37,39,43,71]. Discussions on their tectonic backgrounds continue to this day. For example, the products of the Mongolia-Okhotsk Ocean closure and the Farallon Plate double-subduction [42], the intraplate environment, which is related to the subduction of the Paleo-Pacific plate [43], and the long-range effect of the Mongolia-Okhotsk Ocean closure [91] and so on. In general, the Early Jurassic volcanic rocks all have the characteristics of adakitic rocks, and their genesis is closely related to the basaltic magma underplating event [6,36,37,39,42,43,91].
The Early Jurassic volcanic rocks are mainly a set of intermediate-acidic rock assemblages, including trachyandesite, trachydacite, and a small amount of rhyolite, which are similar to the rock assemblages in the active continental margin environment [92,93]. The major elements indicate that most of the Early Jurassic volcanic rocks belong to the high-K calc-alkaline series of rocks, and a small number of them belong to the alkaline series. The calc-alkaline rock assemblage is considered to be an effective indicator of paleosubduction [38]. The trace elements show that the volcanic rocks are enriched in LREEs and LILEs (such as Ba, Rb, K, Pb), and depleted in HREEs and HFSEs (such as Nb, Ta, P, Ti, Y) (Figure 7), indicating the geochemical characteristics of the igneous rocks in the active continental margin [80,94,95]. In addition, the contemporaneous Early-Middle Jurassic granitic rock assemblages in the Western Liaoning are monzogranite and syenogranite. The major elements indicate by the high-K calc-alkaline series are metaluminous-weakly peraluminous, and is a I type granite. The trace elements are enriched in LREEs and LILEs, depleted in HREEs and HFSEs [96], similar to the geochemical characteristics of volcanic rocks, indicating the geochemical characteristics of igneous rocks in active continental margin similar to volcanic rocks. The common presented strong Nb and Ta depletion (Figure 7) implies in a volcanic island arc tectonic environment associated with subduction. In the tectonic environment discriminant diagram (Figure 10a–c), the samples also show the geodynamic setting of the subducted volcanic island arc, which belongs to the adakitic rock formed by partial melting of the thickened lower crust (Figure 10d), and the active continental margin environment [80,97]. This may be related to the long-range effect of the Paleo-Pacific plate subduction, but the influence of the Mongolia-Okhotsk Ocean closure is not excluded.
Before the Early Jurassic, a large number of fold structures with nearly EW trending and thrust nappes structures with hanging wall pointing to the south were developed in the Eastern Hebei and Western Liaoning. The whole region was under a compressive stress field of nearly SN trend, which may be related to the compressive deformation in the SN direction caused by the subduction of the Paleo-Asian Ocean in the region [51,98,99]. Subsequently, the Early Jurassic entered the joint influence period of the Paleo-Pacific tectonic domain and Mongolian-Okhotsk tectonic domain [38,100,101,102], and the transformation occurred from post-orogenic extension to intracontinental compression orogeny. The regional lower crust thickened under the dual-long-range effect of the Mongolia-Okhotsk Ocean closure and the Paleo-Pacific plate subduction [43,103]. In this thickened lower crust environment, the enriched lithospheric mantle partially melted, and the basaltic magma underplated into the ancient lower crust, resulting in the partial melting to form intermediate-acidic adakitic volcanic rocks (Figure 11).

7. Conclusions

Based on the study of petrography, zircon U–Pb geochronology, geochemistry, and zircon Hf isotope of Early Jurassic volcanic rocks in the Western Liaoning, the following main conclusions were drawn:
(1) The latest zircon U–Pb geochronology results show that in addition to the Early Cretaceous volcanic rocks, a wide range of Early Jurassic intermediate-acidic volcanic rocks also developed in the Xintaimen basin. The formation age is 178.6–181.9 Ma, and the rocks are spatially distributed in the NE direction.
(2) The Early Jurassic volcanic rocks are mainly composed of trachyandesite and a small amount of rhyolite. The geochemical characteristics show high contents of SiO2, Al2O3, and Na2O, high contents of Sr and low contents of Y and Yb, enrichment in LREEs and LILEs, and depletion in HREEs and HFSEs, without Eu anomalies, indicating that they are a set of intermediate-acidic adakitic volcanic rock in high-K calc-alkaline series.
(3) The Early Jurassic Western Liaoning was under the long-range tectonic effects of the closure of the Mongolia-Okhotsk Ocean and the subduction of the Paleo-Pacific plate, which caused the basaltic magma to invade the lower crust of the North China Craton. The mantle-derived magma was separated and crystallized while heating the Proterozoic lower crust, part of the thickened crust melted to form intermediate-acidic adakitic volcanic rocks.

Author Contributions

Z.-W.S., C.-Q.Z. and C.-Y.L. conceived of the presented idea, designed the experiments and verified the data together. The article is originally written and revised by the corresponding author, C.-Q.Z., the other authors are also responsible for many revisions. The financial support for this study was mainly secured by C.-Q.Z., X.-C.X. and C.-Y.L., B.L., Q.-B.W., Y.-L.Z., C.-G.C. and Z.-X.W. digitalized the geological map and performed LA-ICP-MS dating and geochemistry analysis along with Z.-W.S. All authors have read and agreed to the published version of the manuscript.

Funding

This project was financially co-supported by the National Key R&D Program of China (Grant No. 2017YFC0601401), National Natural Science Foundation of China (No. 41472164, 41872192, 41972215 and 41730210), and Self-determined Foundation of Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Natural Resources, China (Grant No. DBY-ZZ-18-09).

Institutional Review Board Statement

Not applicable.

Informed Consent Statement

Not applicable.

Data Availability Statement

The data presented in this study are available in this article.

Acknowledgments

We thank Yujie Hao from the Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Natural Resources, for his kindly help with the analysis of the zircon LA-ICP-MS U-Pb ages. Thanks also due to Qi Zheng from the School of Foreign Language Education, Jilin University, for linguistic review which significantly improved the manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 3. Representative meso- and micro-fabrics of Early Jurassic volcanic rocks. (a) Field outcrops of trachyticdacite. (b) Field outcrop of hornblende trachydacite (hornblende directional arrangement). (c) Trachyte amphibolite dacite (YX-06). (d) Rhyolite (YX-07). Note: Bi—Biotite; Hb—Hornblende; Pl—Plagioclase; Q—Quartz.
Figure 3. Representative meso- and micro-fabrics of Early Jurassic volcanic rocks. (a) Field outcrops of trachyticdacite. (b) Field outcrop of hornblende trachydacite (hornblende directional arrangement). (c) Trachyte amphibolite dacite (YX-06). (d) Rhyolite (YX-07). Note: Bi—Biotite; Hb—Hornblende; Pl—Plagioclase; Q—Quartz.
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Minerals 11 00331 g004 550
Figure 4. Cathodoluminescence images of representative zircons (a,b); Numbers on the images represent analysis spots, and the data near the images represent the associated ages) and 206Pb/238U vs. 207Pb/235U concordia plots of investigated samples (c,d). Errors are 1σ.
Figure 4. Cathodoluminescence images of representative zircons (a,b); Numbers on the images represent analysis spots, and the data near the images represent the associated ages) and 206Pb/238U vs. 207Pb/235U concordia plots of investigated samples (c,d). Errors are 1σ.
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Figure 5. Total-alkali (K2O + Na2O) vs. SiO2 (TAS) diagram (a), after Irvine and Baragar [63]), SiO2 vs. K2O diagram (b), after Peccerillo and Taylor [64]) and Al2O3/(CaO + Na2O + K2O) (A/CNK) vs. Al2O3/(Na2O + K2O) (ANK) diagram (c), after Maniar and Piccoli [65]) diagrams of the Early Jurassic volcanic rocks. F = Foidite; U1 = Tephrite/Basanite; U2 = Phonotephrite; U3 = Tephriphonolite; S1 = Trachybasalt; S2 = Basaltic trachyandesite; S3 = Trachyandesite; T = Trachyte/Trachydacite; Pc = Picrobasal; B = Basalt; O1= Basaltic andesite; O2 = Andesite; O3 = Bacite; R = Rhyolite.
Figure 5. Total-alkali (K2O + Na2O) vs. SiO2 (TAS) diagram (a), after Irvine and Baragar [63]), SiO2 vs. K2O diagram (b), after Peccerillo and Taylor [64]) and Al2O3/(CaO + Na2O + K2O) (A/CNK) vs. Al2O3/(Na2O + K2O) (ANK) diagram (c), after Maniar and Piccoli [65]) diagrams of the Early Jurassic volcanic rocks. F = Foidite; U1 = Tephrite/Basanite; U2 = Phonotephrite; U3 = Tephriphonolite; S1 = Trachybasalt; S2 = Basaltic trachyandesite; S3 = Trachyandesite; T = Trachyte/Trachydacite; Pc = Picrobasal; B = Basalt; O1= Basaltic andesite; O2 = Andesite; O3 = Bacite; R = Rhyolite.
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Figure 6. Variations of major elements vs. SiO2 diagrams (Harker diagrams) of the Early Jurassic volcanic rocks.
Figure 6. Variations of major elements vs. SiO2 diagrams (Harker diagrams) of the Early Jurassic volcanic rocks.
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Minerals 11 00331 g007 550
Figure 7. Primitive mantle normalized trace element spidergrams (a), after Sun and McDonough [66]) and chondrite normalized rare earth element (REE) patterns (b), after Boynton [67]) of the Early Jurassic volcanic rocks.
Figure 7. Primitive mantle normalized trace element spidergrams (a), after Sun and McDonough [66]) and chondrite normalized rare earth element (REE) patterns (b), after Boynton [67]) of the Early Jurassic volcanic rocks.
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Figure 8. Zircon Hf isotopic characteristics of Early Jurassic volcanic rocks in the geological corridor of western Liaoning (a), after Yang et al. [68]; (b), after Wu et al. [69]). CAOB = Central Asian Orogenic Belt; NCC = North China Craton.
Figure 8. Zircon Hf isotopic characteristics of Early Jurassic volcanic rocks in the geological corridor of western Liaoning (a), after Yang et al. [68]; (b), after Wu et al. [69]). CAOB = Central Asian Orogenic Belt; NCC = North China Craton.
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Figure 9. Discriminant diagram of adakite rocks and SiO2 concordant diagram. (a) (La/Yb)N-YbN diagram; (b) Sr/Y-Y diagram; (c) Cr vs. SiO2 diagram; (d) V vs. SiO2 diagram; (e) Cao/Al2O3 vs. SiO2 diagram. (f) Dy/Yb vs. SiO2 diagram.
Figure 9. Discriminant diagram of adakite rocks and SiO2 concordant diagram. (a) (La/Yb)N-YbN diagram; (b) Sr/Y-Y diagram; (c) Cr vs. SiO2 diagram; (d) V vs. SiO2 diagram; (e) Cao/Al2O3 vs. SiO2 diagram. (f) Dy/Yb vs. SiO2 diagram.
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Figure 10. Tectonic discrimination diagrams (a–c) and SiO2-MgO diagram (d), after Lai and Qi [83]) for the Early Jurassic volcanic rocks.
Figure 10. Tectonic discrimination diagrams (a–c) and SiO2-MgO diagram (d), after Lai and Qi [83]) for the Early Jurassic volcanic rocks.
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Figure 11. Tectonic evolution of the northern North China Craton during Early Jurassic (modified after Ma, 2013 [71]). MOO = Mongolia-Okhotsk Ocean; NCC = North China Craton; PPO = Paleo-Pacific Ocean; SC = Siberian Craton; XMOB = Xing’an Mongolian Orogenic Belt; SLB = Solonker-Linxi Suture Belt; YS = Yanshan orogen; TLF = Tan-Lu Fault.
Figure 11. Tectonic evolution of the northern North China Craton during Early Jurassic (modified after Ma, 2013 [71]). MOO = Mongolia-Okhotsk Ocean; NCC = North China Craton; PPO = Paleo-Pacific Ocean; SC = Siberian Craton; XMOB = Xing’an Mongolian Orogenic Belt; SLB = Solonker-Linxi Suture Belt; YS = Yanshan orogen; TLF = Tan-Lu Fault.
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Table
Table 1. LA–ICP–MS zircon U–Pb dating results for the volcanic rocks in the Xintaimen Basin, Western Liaoning.
Table 1. LA–ICP–MS zircon U–Pb dating results for the volcanic rocks in the Xintaimen Basin, Western Liaoning.
Sample No.Th
(ppm)		U
(ppm)		Th/UIsotopic RatioAges (Ma)%U-Pb Disc
207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ207Pb/206Pb1σ207Pb/235U1σ206Pb/238U1σ
YX-06-011261061.180.150300.006868.797090.368720.424510.007702349802317382281351.6
YX-06-023702741.350.166260.0030310.774610.239010.466080.006762520192504212466301.5
YX-06-032354000.590.166400.0033311.430970.233260.494830.00572252219255919259225−1.3
YX-06-044414470.990.050260.003060.211070.012560.030410.000612071001941119340.5
YX-06-051011320.760.056850.007240.227880.030330.030130.001024862362082519168.2
YX-06-061054040.260.158510.002739.987410.203540.453680.007022440162434192412310.9
YX-06-07107613390.800.162920.0028711.117000.209580.491600.00752248614253318257833−1.8
YX-06-084118490.480.048910.001940.139120.005510.020540.0002914466132513120.8
YX-06-09742766321.120.046080.001140.193770.005320.030260.0005222818051923−6.7
YX-06-102962811.050.050310.002740.197800.010780.028810.0005020994183918330.0
YX-06-1110,36678251.320.048740.000860.189940.003920.028050.000401352417731783−0.6
YX-06-1214919291.600.051650.002090.192760.006870.027290.0003627057179617422.8
YX-06-13238111282.110.049170.002920.143420.008480.021220.0004215698136813530.7
YX-06-14513616103.190.049640.002190.200560.008750.029220.0004517873186718630.0
YX-06-1514637851.860.051130.001830.205640.007540.029020.0003624762190618423.2
YX-06-161071280.840.052750.007290.192270.021460.027980.000873181951791817850.6
YX-06-179829631.020.049670.001870.197400.007490.028750.0003918063183618320.0
YX-06-18306428201.090.048730.001320.191610.005180.028510.000381353917841812−1.7
YX-06-192572850.900.051250.003230.190070.012270.026940.000522521131771017133.4
YX-06-202473150.780.056190.003290.217880.012150.028590.00048460942001018239.0
YX-06-21848661801.370.049840.000840.200480.003570.029110.0003218822186318520.5
YX-06-223784000.940.165060.0024710.758590.183600.470980.005582508142502162488240.6
YX-06-23203921020.970.049660.001290.194370.005240.028360.0004317936180418030.0
YX-06-24286828061.020.049610.004080.141200.011320.020640.000381771871341013221.5
YX-06-2541312000.340.160810.002489.488830.167540.427050.005062464152386162292233.9
YX-07-019878081.220.051010.001910.133430.005300.019120.0004024154127512233.9
YX-07-026154231.460.046050.003830.180940.014420.028500.00068 183169121814−7.1
YX-07-03310021611.430.048780.001320.189990.005440.028890.000741373017751845−4.0
YX-07-049819641.020.050160.002160.207000.009840.030130.0009120258191819160.0
YX-07-053705060.730.160970.002808.645940.205830.392760.009172466182301222136427.2
YX-07-06348323791.460.051030.002220.129340.005550.018800.0006524245124512043.2
YX-07-07141610571.340.051260.001750.193800.006350.027870.0005225342180517731.7
YX-07-086366610.960.050800.002120.215360.008790.031110.0005323263198719830.0
YX-07-09125715840.790.053040.001650.206520.007890.028100.0006833146191717946.3
YX-07-10166218070.920.049640.001310.198860.005950.028930.0004817840184518430.0
YX-07-117077280.970.049900.001880.191170.006990.027880.0003319063178617720.6
YX-07-124174910.850.051210.002830.196690.009630.028350.0004225085182818031.1
YX-07-13247121951.130.049720.001630.185380.006430.026930.0004218252173617131.2
YX-07-146094041.510.050140.003090.187860.011330.027410.000532011031751017430.6
YX-07-159349960.940.050170.001600.194440.006370.028090.0003920350180517920.6
YX-07-166007210.830.050180.001840.197550.007340.028490.0003520463183618121.1
YX-07-173814750.800.054680.002450.211810.008770.028420.0004839962195718137.2
YX-07-186147840.780.050290.001710.192110.006270.027930.0003620951178517820.0
YX-07-198169720.840.051580.001670.203130.007040.028580.0004326752188618233.2
YX-07-204894841.010.053880.003410.199020.012000.027070.00058366971841017246.5
YX-07-2148512160.400.151840.002257.162320.127060.341030.0040923671521321618922011.3
YX-07-224956010.820.049660.002130.194550.009070.028220.0004717977181817931.1
YX-07-23112013590.820.050070.001840.198150.006760.028870.0003719855184618320.5
YX-07-244084760.860.049800.003000.181280.011010.026550.00051186104169916930.0
YX-07-25152910011.530.058420.002070.224930.007670.028050.00036546522066178213.6
Table
Table 2. Major elements (wt.%) compositions for the Early Jurassic volcanic rocks.
Table 2. Major elements (wt.%) compositions for the Early Jurassic volcanic rocks.
Sample No.LithologySiO2TiO2Al2O3TFeOMnOMgOCaONa2OK2OP2O5LOITotalMg#Na2O + K2OA/CNKA/NK
N17-1Trachydacite68.590.3715.482.690.030.510.7654.960.151.46100.2925.39.961.031.14
N17-2Trachydacite69.670.3615.512.490.040.272.074.284.530.160.82100.4516.18.810.991.30
N18-2Trachydacite67.280.3816.242.710.040.491.415.074.50.161.7100.2724.29.571.031.23
N19-1Trachydacite67.440.3716.062.60.040.411.545.224.270.161.86100.2421.89.491.001.22
N20-2Trachydacite69.050.3415.592.540.030.31.196.013.350.161.38100.2217.29.360.991.15
N21-1Trachydacite660.5215.394.510.071.782.113.953.820.32.42101.3741.37.771.061.45
N22-1Trachydacite67.050.3615.342.880.050.551.844.354.430.172.96100.2925.58.781.001.28
N23-1Rhyolite71.450.2814.232.690.030.571.173.975.020.111.02100.8427.48.991.011.19
YX-06Trachydacite65.470.4115.293.380.081.6623.464.340.193.9100.5446.77.81.091.47
YX-07Rhyolite71.390.2814.412.440.060.40.634.3550.11.26100.5822.59.351.051.15
YX-08Trachydacite68.90.2415.162.430.20.651.614.154.730.092.12100.5632.48.881.021.27
S5234 Rhyolite 71.130.2314.932.050.060.421.624.344.350.080.8100.2326.78.691.011.26
Table
Table 3. Trace elements for the Early Jurassic volcanic rocks.
Table 3. Trace elements for the Early Jurassic volcanic rocks.
Sample No.N17-1N17-2N18-2N19-1N20-2N21-1N22-1N23-1YX-06YX-07YX-08S5234
Cr9.056.955.665.846.4710.913.26.7626.511.56.908.49
Ni2.032.582.212.393.909.346.313.9115.44.342.232.82
Sc1.922.542.342.232.634.423.002.724.172.613.012.34
Co3.552.843.893.663.667.544.963.426.953.583.292.83
V34.836.132.435.030.550.336.128.945.923.320.824.8
Ba14591529156514029261451133012991493907915947
Rb11911311510976.495.811915011313393.488.4
Th3.294.574.444.033.924.804.0010.54.597.833.232.92
U0.891.451.101.111.091.371.191.771.121.700.580.81
Nb12.511.912.212.515.314.013.310.412.610.49.759.05
Ta0.931.011.011.001.131.081.101.060.970.830.620.76
Sr541748800865458632695453565156340395
Zr157152157155150153153165152165120113
Hf8.027.267.056.546.906.746.305.506.144.756.424.17
Y5.76.06.87.27.57.27.36.47.46.06.815.95
Pb15.617.818.817.818.719.717.524.618.119.717.018.0
Ga15.217.818.417.518.618.815.616.318.613.316.316.2
Cs1.081.711.441.220.961.141.361.952.720.900.470.67
La13.6225.3131.4631.3731.0033.3318.1932.1224.1529.5420.2017.58
Ce36.6754.0559.7564.1061.8566.3047.1868.4056.4261.9843.2140.87
Pr4.956.177.107.176.858.116.117.466.646.375.434.85
Nd17.8720.3823.0323.2922.1126.9421.5122.6922.4619.4217.9016.30
Sm2.923.253.323.403.444.153.643.523.672.912.672.52
Eu0.840.951.041.050.931.291.010.831.120.650.810.67
Gd2.472.773.013.012.983.522.902.612.882.522.462.29
Tb0.290.300.320.350.350.380.340.320.340.270.290.26
Dy1.311.331.461.531.611.691.631.401.621.231.371.20
Ho0.220.220.260.250.270.280.270.250.280.230.250.20
Er0.580.640.680.770.790.790.780.670.810.640.690.64
Tm0.090.100.100.100.120.110.110.110.110.090.110.10
Yb0.550.650.650.700.750.700.730.660.710.600.720.62
Lu0.090.100.090.110.110.100.110.100.100.090.110.10
Eu*0.930.950.990.990.871.010.920.801.020.710.950.84
Sr/Y94.28123.59117.94120.2860.8287.4994.9170.8176.2425.8049.8666.48
ΣREE821161321371331481051411211279688
(La/Yb)N16.7026.4032.5530.3727.9732.2716.7432.7922.8933.1018.9819.25
Nb/Ta13.5211.7712.0512.5513.5612.9612.159.7813.0412.5515.7111.93
(Gd/Yb)N3.633.463.733.493.214.083.193.193.273.382.773.00
Ce/Pb2.353.043.193.603.313.372.692.783.123.152.542.27
Nb/U14.168.2511.1111.2814.0310.2211.265.8511.296.1016.7311.22
Table
Table 4. Zircon Hf isotopic data for the Early Jurassic volcanic rocks.
Table 4. Zircon Hf isotopic data for the Early Jurassic volcanic rocks.
Sample No.t (Ma)176Yb/177Hf176Lu/177Hf176Hf/177Hf2σεHf(0)εHf(t)2σTDM1TDM2fLu/Hf
YX-06 011810.0175620.0007320.2822670.000024−17.9−14.00.913812109−0.98
YX-06 021740.1596030.0062900.2826190.000029−5.4−2.31.010421363−0.81
YX-06 031810.0729340.0028110.2823390.000026−15.3−11.70.913531961−0.92
YX-06 041810.0360050.0014160.2823140.000022−16.2−12.40.813392008−0.96
YX-06 051810.0244570.0009800.2823330.000016−15.5−11.70.612971963−0.97
YX-06 061810.0133960.0005540.2822860.000020−17.2−13.30.713472063−0.98
YX-06 071810.1013190.0042420.2822220.000021−19.4−16.00.715882232−0.87
YX-06 081810.0409070.0016880.2822780.000016−17.5−13.70.613992090−0.95
YX-07 011780.0269830.0012250.2823370.000021−15.4−11.60.713001958−0.96
YX-07 021780.0186330.0007880.2823760.000020−14.0−10.20.712311868−0.98
YX-07 031780.0256970.0011210.2823680.000019−14.3−10.50.712521887−0.97
YX-07 041780.0214620.0010110.2823840.000020−13.7−9.90.712271851−0.97
YX-07 051780.0313380.0014020.2823970.000018−13.3−9.50.612211824−0.96
YX-07 061780.0418230.0016940.2824570.000025−11.1−7.40.911451692−0.95
YX-07 071780.0393030.0018100.2823780.000020−13.9−10.20.712611869−0.95
YX-07 081780.0179710.0007700.2824250.000016−12.3−8.50.611621758−0.98
YX-07 091780.0229840.0010020.2824160.000019−12.6−8.80.711811779−0.97
YX-07 101780.0328370.0014630.2823410.000021−15.2−11.50.813011949−0.96
YX-07 111780.0270100.0012960.2824080.000017−12.9−9.10.612021799−0.96
YX-07 121780.0271950.0011810.2824020.000018−13.1−9.30.612061811−0.96
YX-07 141780.0285100.0011980.2824030.000021−13.0−9.30.712061809−0.96
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Song, Z.-W.; Zheng, C.-Q.; Liang, C.-Y.; Lin, B.; Xu, X.-C.; Wen, Q.-B.; Zhao, Y.-L.; Cao, C.-G.; Wang, Z.-X. Identification and Geological Significance of Early Jurassic Adakitic Volcanic Rocks in Xintaimen Area, Western Liaoning. Minerals 2021, 11, 331. https://doi.org/10.3390/min11030331

AMA Style

Song Z-W, Zheng C-Q, Liang C-Y, Lin B, Xu X-C, Wen Q-B, Zhao Y-L, Cao C-G, Wang Z-X. Identification and Geological Significance of Early Jurassic Adakitic Volcanic Rocks in Xintaimen Area, Western Liaoning. Minerals. 2021; 11(3):331. https://doi.org/10.3390/min11030331

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Song, Zhi-Wei, Chang-Qing Zheng, Chen-Yue Liang, Bo Lin, Xue-Chun Xu, Quan-Bo Wen, Ying-Li Zhao, Cheng-Gang Cao, and Zhi-Xin Wang. 2021. "Identification and Geological Significance of Early Jurassic Adakitic Volcanic Rocks in Xintaimen Area, Western Liaoning" Minerals 11, no. 3: 331. https://doi.org/10.3390/min11030331

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