Home Permian tectonic switch of the southern Central Asian Orogenic Belt: Constraints from magmatism in the southern Alxa region, NW China
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Permian tectonic switch of the southern Central Asian Orogenic Belt: Constraints from magmatism in the southern Alxa region, NW China

  • Erteng Wang , Xinwei Zhai EMAIL logo , Yaoshen Huang , Chengze Li , Ruihuan Su , Lei Wu , Gaorui Song , Zhiang Guo , Wanfeng Chen and Jinrong Wang
Published/Copyright: March 16, 2024
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Open Geosciences
From the journal Open Geosciences Volume 16 Issue 1

Abstract

Late Paleozoic plutons are widely distributed in the Alxa region, southernmost Central Asian Orogenic Belt, and provided an important clue in constraint for the closing time of the Paleo-Asian Ocean (PAO). In this article, we present new zircon U-Pb ages and whole-rock geochemical data from the Permian Huoersen and Zongnaishan plutons in the southern Alxa region. The Huoersen gabbro (ca. 285 Ma) is enriched in large-ion lithophile elements and depleted in high-field strength elements, similar to the features of continental marginal arc. They were most likely generated by partial melting of depleted mantle that was modified by subduction metasomatic fluids. The Zongnaishan granites (ca. 267 Ma) show characteristics of I-type granites and were generated in a syn-collision setting. The Huoersen granites (ca. 259 Ma) are peralkaline and have positive Ɛ Nd(t) (+1.2 to +1.5) values, exhibiting A2-subtype granites affinities. They were formed by melting of lower crust in post-collision extension setting. Based on geodynamic mechanism, a three-stage evolution model is delineated: subduction, syn-collision to post-collisional extension for oceanic branch of the PAO during the Permian. In general, the rock assemblages indicate a tectonic switch from subduction to post-collision extension regimes and the final closure of the PAO.

Keywords: geochemical; Permian; tectonic switch; Alxa region; Central Asian Orogenic Belt

1 Introduction

Plate tectonic is the predominant process of global tectonic, and its main forms are oceanic subduction-closure and subsequently continental collision [1,2,3]. The Central Asian Orogenic Belt (CAOB), one of the largest mega-accretive orogenic belts in the world, is bounded by the Eastern European Craton to the east, the Tarim Craton and North China Craton to the south, and the Siberia Craton to the north (Figure 1a) [4,5,6,7]. The CAOB is a collage of geological bodies formed in subduction closure of the Paleo-Asian Ocean (PAO) during Neoproterozoic to Mesozoic, which is regarded as one of the significant geological events during the global plate tectonic [8,9,10,11]. Recent researches show the PAO was finally closed in the Tianshan-Solonker suture zone, southern CAOB [12]. However, compared with the eastern and western parts of the CAOB [13,14,15,16,17,18,19,20], less attentions are paid for the middle part and further study is vital and necessary.

Figure 1 (a) The location of the Alxa region in the simplified tectonic sketch map of the Central Asian Orogenic Belt (modified after [5]). (b) Tectonic outline of the surrounding Alxa in North China (modified after [64]). (c) Geological map of the Alxa region (YTZ – Yagan tectonic zone, ZHTZ – Zhusileng-Hangwula tectonic zone, ZSTZ – Zongnaishan-Shalazhashan tectonic zone, NLTZ – Nuoergong–Langshan tectonic zone, modified after [71]).
Figure 1

(a) The location of the Alxa region in the simplified tectonic sketch map of the Central Asian Orogenic Belt (modified after [5]). (b) Tectonic outline of the surrounding Alxa in North China (modified after [64]). (c) Geological map of the Alxa region (YTZ – Yagan tectonic zone, ZHTZ – Zhusileng-Hangwula tectonic zone, ZSTZ – Zongnaishan-Shalazhashan tectonic zone, NLTZ – Nuoergong–Langshan tectonic zone, modified after [71]).

The Alxa region is located in the southernmost margin of the middle CAOB (Figure 1a) and bounded by the Solonker suture zone to the east and Tianshan-Beishan suture zone to the west (Figure 1b) [12,21]. Magma and tectonic activities of the Alxa are strong, and it is characterized by an abundance of the acid and mafic-ultramafic magmatism (Figure 1c) [20,22,23]. For a long time, the closure time of the PAO in the Alxa region has been highly controversial, such as in the middle to late Devonian [24], or late Carboniferous to early Permian [20,25,26], and subduction of the PAO until the middle Permian to early Triassic [27] (and others references). Notably, the Paleozoic tectonic transformation from subduction to post-collision was widely manifested by magmatism related to subduction and closure of the PAO in the southern Alxa region [22,28,29]. So, to better constrain the timing of subduction and closure of the PAO, a detailed study of Alxa region rocks’ assemblage is important.

Here, we report continental marginal arc gabbro, I- and A-type granites about subduction, syn-collision to post-collision setting in the Zongnaishan-Shalazhashan, southern Alxa region. We present geochronological, geochemical, and Sr–Nd–Hf isotopic data for the granite and gabbro. We further discuss their petrogenesis and the deep-level processes relating to the magmatic activity and thus provide constraints on the evolution of the Alxa region and the timing of the closure of the PAO branch.

2 Geological setting

The Alxa region, belonging to the southernmost part of the CAOB (Figure 1a), is located at the intersection of Tarim Craton, North China Craton, and Qilian Orogenic belt, which was initially regarded as an eastern extension of the North China Craton (Figure 1b) [30,31]. In particular, through the restoration of metamorphic, paleomagnetism, and mélange, the Alxa region showed an inconsistent tectonic history with the North China Craton [32].

The Alxa region has four major tectonic zones, e.g. Yagan tectonic zone, Zhusileng-Hangwula tectonic zone, Zongnaishan-Shalazhashan tectonic zone, and Nuoergong–Langshan tectonic zone from north to south, and divided by three major faults and ophiolite belts: the Yagan fault, the Enger Us fault (ophiolite belt), and the Qugan Qulu fault (ophiolite belt) (Figure 1c). The Enger Us Ophiolite Belt might represent the major oceanic branch of the PAO, with the age of 300 Ma [33,34], while the Qugan Qulu Ophiolite Belt (ca. 275 Ma) [34] is a back arc basin, which is formed by the southward subduction of branch PAO and had closed during the late Paleozoic [10,27,35].

In the southern Alxa region, the desert-covered area has a crystalline basement of Neoproterozoic Granite gneiss, which is mainly distributed in Nuoergong–Langshan tectonic zone [36]. The limestone and dolomite of Cambrian to Ordovician are sparsely distributed, while the Upper Paleozoic strata are very common (Figure 1c). The Devonian strata are clastic-carbonate sedimentary formation of neritic facies, and the Carboniferous to Permian strata major are conglomerate, sandstone, carbonate rock, volcanic rock, and pyroclastic rock [30,37].

Late Paleozoic Granites are widespread with less basic rocks in the Alxa region (Figure 1c). The corresponding tectonic environments are of great dispute, and previous studies gave different ideas: active continental margin environment [19,23,35,38], the intraplate setting [39], or post-collision extensional environment [20].

3 Sample descriptions

The Huoersen pluton and the Zongnaishan pluton are located at the Zongnaishan-Shalazhashan tectonic zone, south of the Enger Us Ophiolite Belt (Figure 1c). The Huoersen pluton consists of granite and gabbro, and the gabbro was intruded into by granite (Figure 2a). The Zongnaishan pluton consists of granites and intruded into the Carboniferous strata (Figure 2b). We sampled Huoersen granite, Huoersen gabbro, and Zongnaishan granite for analysis of geochronology and whole rocks geochemistry.

Figure 2 (a) Geological map of the Huoersen pluton (modified after geological map of 1:200,000). (b) Geological map of the Zongnaishan pluton (modified after geological map of 1:200,000).
Figure 2

(a) Geological map of the Huoersen pluton (modified after geological map of 1:200,000). (b) Geological map of the Zongnaishan pluton (modified after geological map of 1:200,000).

The grayish-black Huoersen gabbros (Figure 3a) with gabbro-structure are mainly composed of plagioclase (55%), pyroxene (20%), amphibole (20%), and iron (<5%). The plagioclase grain is euhedral to subhedral. The pyroxene is allotriomorphic granular and filled in the interspace of plagioclase, and partly chloritized. The hornblende is idiomorphic and semi-idiomorphic (Figure 3b). The Huoersen granites are flesh-red and massive-structure, and mainly composed of plagioclase (45%), quartz (35%), K-feldspar (10%), and biotite (5%) and a few accessory minerals of zircon and iron (<5%). The biotite grain occurred in the form of inclusion (Figure 3c and d). The fresh Zongnaishan granite is flesh-red (Figure 3e), with medium granitic texture and massive structure. The main mineral composition is potassium feldspar (40%), plagioclase (10%), quartz (35%), biotite (5–10%), and a small amount of amphibole (<5%) (Figure 3f).

Figure 3 Representative field photographs and photomicrographs. (a and b) For the Huoersen gabbro. (c and d) For the Zongnaishan granite. (e and f) For the Huoersen granite. Mineral abbreviations: Qtz, quartz; Pl, plagioclase; Bt, biotite; Mus, muscovite; Am, amphibole; Kfs, K-feldspar; Px: pyroxene.
Figure 3

Representative field photographs and photomicrographs. (a and b) For the Huoersen gabbro. (c and d) For the Zongnaishan granite. (e and f) For the Huoersen granite. Mineral abbreviations: Qtz, quartz; Pl, plagioclase; Bt, biotite; Mus, muscovite; Am, amphibole; Kfs, K-feldspar; Px: pyroxene.

4 Analytical methods

Zircon cathodoluminescence (CL) images were obtained at the Langfang Chenxin Geological Service Co., Hebei, China. U-Pb dating, whole-rock major, trace element, and Sr-Nd-Hf isotope analyses were performed at the Key Laboratory of Mineral Resources in Western China, Lanzhou University, Lanzhou, China.

4.1 Zircon U-Pb dating

After separation by conventional heavy liquid and magnetic techniques, zircon grains from studied samples were hand-picked and embedded in an epoxy mount under a binocular microscope and then polished to expose half of the zircon grains. The U-Pb isotope ratios of the selected zircons were measured using an Agilent 7500X inductively coupled plasma mass spectrometry (ICP-MS) instrument combined with a Geo-Las200M laser ablation (LA) system. The zircon standard 91500 [40] was used as the age standard. The reference glass NIST 610 [41] and Si were applied as external and internal standards, respectively. The spot diameter was ∼30 μm and the analytical techniques are referred to [42]. Data reduction was performed using the Glitter (ver. 4.0) program, and common Pb was corrected using the common lead correction program [41]. Concordia plots and weighted mean ages were generated using the Isoplot program [43]

4.2 Major and trace element analyses

Major element compositions were analyzed by ICP optical emission spectroscopy. The analytical accuracy was better than 2%. The loss on ignition (LOI) was obtained by heating approximately 0.5 g of dried sample powder at 1,000°C for 2 h. Trace element contents were analyzed by ICP-MS on an Agilent 7700X instrument, and the analytical errors were less than 10%. The US Geological Survey reference materials AGV-2 and BCR-2 were used as standards.

4.3 Whole-rock Sr-Nd-Hf isotopic

The rock samples’ powders were mixed with 0.5 ml 60 wt% HNO3 and 1.0 ml 40 wt% HF in high-pressure PTFE bombs. These bombs were steel-jacketed and placed in the oven at 195℃ for 3 days for digestion. The digested samples were then dried on a hotplate at 150℃ for 2 h and reconstituted in 1.5 ml of 1.5 N HCl before ion exchange purification. The analytical procedure was the same as that described by [44]. The diluted solution was introduced into a Nu Instruments Nu Plasma II MC-ICP-MS (Wrexham, Wales, UK) through a Teledyne Cetac Technologies Aridus II desolating nebulizer system (Omaha, Nebraska, USA). Raw data of isotopic ratios were internally corrected for mass fractionation by normalizing to 86Sr/88Sr = 0.1194, 146Nd/144Nd = 0.7219 for Nd, and 179Hf/177Hf = 0.7325 for Hf with exponential law. International isotopic standards (NIST SRM 987 for Sr, JNdi-1 for Nd, Alfa Hf) were periodically analyzed to correct instrumental drift. Geochemical reference materials of USGS BCR-2, BHVO-2, AVG-2, and RGM-2 were treated as quality control.

5 Results

5.1 Zircon U-Pb age

The LA-ICP-MS zircon dating results of Huoersen granite, Huoersen gabbro, and Zongnaishan granite from the Alxa region are given in Table 1.

Table 1

Zircon LA-ICP-MS U-Pb isotopic data of the Huoersen and Zongnaishan pluton in the southern Alxa region

Spot no. Isotopic ratios Ages (Ma)
207Pb/235U 206Pb/238U 207Pb/235U 206Pb/238U
Ratios ±1σ Ratios ±1σ Age ±1σ Age ±1σ
Huoersen gabbro
16HEN1-1 0.33537 0.00414 0.04505 0.00056 294 3 284 3
16HEN1-2 0.34448 0.00698 0.04534 0.00058 301 5 286 4
16HEN1-3 0.30928 0.00395 0.04548 0.00056 274 3 287 3
16HEN1-4 0.33601 0.0044 0.04489 0.00055 294 3 283 3
16HEN1-5 0.32553 0.00833 0.04505 0.00058 286 6 284 4
16HEN1-6 0.33971 0.00761 0.04544 0.00056 297 6 286 3
16HEN1-7 0.31949 0.00709 0.04495 0.00056 282 5 283 3
16HEN1-8 0.34199 0.00398 0.04539 0.00052 299 3 286 3
16HEN1-9 0.30707 0.0058 0.04544 0.00053 272 5 286 3
Zongnaishan granite
16ZN1-1 0.31475 0.01218 0.04104 0.00106 278 10 259 6
16ZN1-2 0.29263 0.01258 0.04225 0.00112 261 10 267 6
16ZN1-3 0.30369 0.0133 0.04267 0.00114 269 10 269 8
16ZN1-4 0.31630 0.01188 0.04260 0.00112 279 10 269 6
16ZN1-5 0.31847 0.01432 0.04309 0.00118 281 12 272 8
16ZN1-6 0.30383 0.01082 0.04204 0.0011 269 8 265 6
16ZN1-7 0.32037 0.0146 0.04278 0.00118 282 12 270 8
16ZN1-8 0.29858 0.0124 0.04129 0.00112 265 10 261 6
16ZN1-9 0.31734 0.0131 0.04398 0.00120 280 10 277 8
16ZN1-10 0.33119 0.01528 0.04213 0.00120 290 12 266 8
16ZN1-11 0.32052 0.0137 0.04364 0.00120 282 10 275 8
16ZN1-12 0.33054 0.01488 0.04303 0.00118 290 12 272 8
16ZN1-13 0.31241 0.01442 0.04228 0.00118 276 12 267 8
16ZN1-14 0.31095 0.0132 0.04254 0.00114 275 10 269 8
16ZN1-15 0.29175 0.01294 0.04144 0.00112 260 10 262 6
16ZN1-16 0.31947 0.01336 0.04283 0.00114 281 10 270 8
16ZN1-17 0.30283 0.01292 0.04274 0.00114 269 10 270 8
Huoersen granite
16HEN7-1 0.29175 0.00513 0.04173 0.00046 260 4 264 3
16HEN7-2 0.29309 0.00469 0.0411 0.00045 261 4 260 3
16HEN7-3 0.28699 0.00623 0.0408 0.00046 256 5 258 3
16HEN7-4 0.29099 0.00395 0.04097 0.00045 259 3 259 3
16HEN7-5 0.29202 0.00389 0.04087 0.00044 260 3 258 3
16HEN7-6 0.29011 0.0058 0.04083 0.00046 259 5 258 3
16HEN7-7 0.28892 0.00725 0.04092 0.00048 258 6 259 3
16HEN7-8 0.2923 0.00387 0.04074 0.00044 260 3 257 3
16HEN7-9 0.29053 0.00414 0.04121 0.00045 259 3 260 3
16HEN7-10 0.29147 0.00442 0.04101 0.00045 260 3 259 3
16HEN7-11 0.29047 0.00385 0.04071 0.00044 259 3 257 3
16HEN7-12 0.28973 0.00414 0.0406 0.00044 258 3 257 3
16HEN7-13 0.29017 0.00391 0.04058 0.00044 259 3 256 3
16HEN7-14 0.29157 0.00445 0.04091 0.00045 260 3 258 3
16HEN7-15 0.28985 0.00382 0.04094 0.00045 258 3 259 3
16HEN7-16 0.29205 0.00519 0.04161 0.00046 260 4 263 3
16HEN7-17 0.29679 0.00528 0.04189 0.00047 264 4 265 3
16HEN7-18 0.29331 0.00394 0.04132 0.00045 261 3 261 3
16HEN7-19 0.2898 0.00376 0.04101 0.00045 258 3 259 3

5.1.1 Huoersen gabbro

The zircons from the Huoersen gabbro are 100–150 μm long euhedral, in which ratios of length to width vary from 1:1 to 1:2. The CL image of zircons has obvious concentric oscillatory zoning (Figure 4a) and high Th/U ratios (0.28–2.16), indicating a magmatic origin [44]. The nine zircons from Huoersen gabbro were analyzed for U-Pb ages, with a 206Pb/238U weighted mean age of 285.0 ± 2.1 Ma (mean square of weighted deviates [MSWD] = 0.24) (Figure 4a).

Figure 4 Representative CL images and zircon U–Pb concordia diagram for the samples from the southern Alxa region. (a) Huoersen gabbro. (b) Zongnaishan granite. (c) Huoersen granite.
Figure 4

Representative CL images and zircon U–Pb concordia diagram for the samples from the southern Alxa region. (a) Huoersen gabbro. (b) Zongnaishan granite. (c) Huoersen granite.

5.1.2 Zongnaishan granite

The zircons from Zonnaishan granites show subhedral granular with sizes ranging from 50 to 70 μm and have dark bands in the CL image (Figure 4b). Seventeen zircons for Zongnaishan granite were analyzed. The Th/U ratios from 0.22 to 2.65 indicate the characteristics of magmatic zircons [45]. Seventeen zircon ages ranged from 259 ± 6 to 277 ± 8 Ma, with a weighted mean age of 267.3 ± 3.5 Ma (MSWD = 1.9) (Figure 4b).

5.1.3 Huoersen granite

The zircon from the Huoersen granites shows euhedral to subhedral with sizes ranging from 50 to 150 μm and has oscillatory zoning in the CL image (Figure 4c). Twenty zircons for granite were analyzed. They have high Th/U ratios (0.36–0.68), which are characteristics of magmatic zircons [45]. Nineteen zircon analyses yielded concordant 206Pb/238U ages ranging from 257 ± 3 to 265 ± 3 Ma, 207Pb/235U ages ranging from 256 ± 3 to 264 ± 4 Ma, with a concordant 206Pb/238U age of 259.1 ± 0.51 Ma (MSWD = 0.091) (Figure 4c).

5.2 Whole-rock major and trace element composition

Whole-rock major and trace element compositions of all samples from Huoersen granite and gabbro and Zongnaishan granite are given in Table 2.

Table 2

Whole-rock major (wt%) and trace element (ppm) analyses of samples from the Huoersen and Zongnaishan plutons

Rock type Huoersen gabbro Zongnaishan granite Huoersen granite
Samples 16HE-1 16HE-2 16HE-3 16HE-4 16HE-5 16HE-6 16HE-7 16HE-8 16HE-9 16HE-10 16HE-11 16HE-12 16ZN-1 16ZN-2 16ZN-3 16ZN-4 16ZN-5 16ZN-6 16ZN-7
SiO2 47.66 48.31 46.82 47.74 45.73 45.88 67.32 67.91 68.00 68.23 69.87 67.98 75.13 75.31 74.78 74.86 77.44 75.97 75.82
TiO2 1.90 1.91 2.00 1.76 1.84 1.87 15.73 16.04 16.18 15.99 15.83 15.72 0.20 0.21 0.18 0.18 0.19 0.18 0.19
Al2O3 14.39 15.43 14.64 16.50 16.01 16.06 0.38 0.39 0.33 0.30 0.36 0.32 12.35 12.25 11.84 12.22 11.61 12.01 11.82
Fe2O3 8.71 8.47 8.92 7.94 9.18 8.71 3.15 2.93 2.63 2.56 2.82 2.87 1.71 1.66 1.60 1.41 1.59 1.36 1.72
MgO 8.62 7.11 7.36 7.05 6.96 7.65 0.06 0.05 0.05 0.05 0.05 0.06 0.22 0.17 0.17 0.15 0.19 0.13 0.17
BaO 0.14 0.13 0.12 0.14 0.11 0.14 0.60 0.59 0.61 0.61 0.55 0.54 0.02 0.02 0.01 0.01 0.01 0.01 0.01
CaO 10.96 10.76 11.54 9.86 12.74 11.11 2.07 1.60 1.63 1.60 1.52 1.96 0.23 0.63 0.61 0.70 0.61 0.62 0.52
Na2O 3.39 3.47 3.42 4.50 4.06 3.90 3.86 3.91 4.03 4.01 3.88 3.78 4.04 3.96 3.78 3.94 3.46 3.82 3.81
K2O 1.96 1.60 1.53 1.91 1.19 2.03 4.45 4.38 4.66 4.50 4.47 4.54 5.57 5.55 5.42 5.72 4.52 5.39 5.41
P2O5 1.59 1.36 1.63 1.53 1.82 1.54 0.14 0.11 0.17 0.10 0.09 0.10 0.05 0.03 0.01 0.02 0.02 0.03 0.05
LOI 1.32 1.75 1.60 1.83 1.60 1.68 1.51 0.95 0.76 0.91 0.87 1.36 0.61 0.70 0.68 0.71 0.98 0.74 0.89
Total 100.63 100.30 99.57 100.78 101.24 100.58 99.27 98.86 99.05 98.86 100.31 99.23 100.12 100.47 99.09 99.92 100.61 100.27 100.42
Mg# 63.81 59.94 59.55 61.29 57.46 61.02 27.44 28.56 31.53 32.11 27.91 27.20 18.33 15.49 16.02 15.83 17.58 14.24 14.64
La 107 79.74 89.57 127 126 89.29 50.70 67.60 27.20 28.70 54.90 45.20 53.99 54.73 45.85 44.19 49.25 45.30 52.00
Ce 186 185 213 219 204 200 109 140 55.90 58.50 113.50 95.70 108 112 101 90.04 108 101 107
Pr 23.98 24.05 28.11 27.48 25.14 25.43 12.75 16.05 6.39 6.88 12.95 11.05 13.61 14.01 11.72 11.24 12.54 11.76 13.12
Nd 101 101 118 112 104 105 48.20 59.40 24.10 26.30 48.20 42.00 51.30 53.12 44.25 42.52 47.51 44.49 49.65
Sm 16.71 16.69 19.75 17.83 16.93 17.34 9.44 11.05 4.95 5.44 9.14 8.14 10.42 10.89 9.16 8.80 9.68 9.23 10.06
Eu 4.16 4.29 4.78 4.32 4.26 4.31 0.77 0.92 0.72 0.73 0.88 0.86 0.55 0.56 0.51 0.47 0.54 0.51 0.52
Gd 10.96 10.72 12.54 11.29 10.84 10.82 6.67 7.98 4.04 4.07 6.57 5.88 9.72 10.26 8.76 8.32 8.92 8.47 9.20
Tb 1.22 1.22 1.37 1.29 1.20 1.21 0.83 0.93 0.54 0.53 0.81 0.71 1.62 1.73 1.49 1.41 1.51 1.42 1.56
Dy 5.78 5.57 6.37 5.92 5.62 5.63 3.91 4.32 2.91 2.69 3.78 3.23 10.17 11.03 9.41 8.97 9.37 9.04 9.74
Ho 0.96 0.91 1.06 0.97 0.90 0.94 0.60 0.65 0.50 0.44 0.59 0.47 2.08 2.26 1.95 1.84 1.90 1.84 1.98
Er 2.44 2.34 2.64 2.52 2.42 2.39 1.33 1.48 1.32 1.07 1.32 1.06 6.17 6.80 5.95 5.64 5.77 5.62 6.05
Tm 0.29 0.28 0.32 0.32 0.29 0.29 0.17 0.18 0.19 0.16 0.16 0.13 0.86 0.99 0.87 0.81 0.82 0.83 0.89
Yb 1.77 1.71 1.96 1.91 1.76 1.78 1.05 1.07 1.22 0.99 1.04 0.82 5.70 6.62 5.69 5.34 5.68 5.69 6.02
Lu 0.26 0.24 0.28 0.29 0.26 0.26 0.15 0.16 0.18 0.15 0.15 0.12 0.84 0.97 0.85 0.80 0.84 0.85 0.87
ΣREE 464 434 501 534 504 465 261 329 144 148 269 227 275 286 247 230 262 246 269
LREE 440 411 474 510 481 442 231 295 119 126 239 202 238 246 212 197 227 212 233
HREE 23.69 22.99 26.52 24.51 23.28 23.33 30.41 34.07 25.10 22.30 30.02 24.62 37.15 40.66 34.97 33.13 34.80 33.76 36.30
LREE/HREE 18.59 17.91 17.90 20.81 20.66 18.98 7.61 8.66 4.75 5.67 7.98 8.24 6.43 6.05 6.09 5.95 6.54 6.31 6.43
δEu 0.88 0.92 0.87 0.87 0.90 0.90 0.30 0.30 0.49 0.47 0.35 0.38 0.17 0.16 0.17 0.17 0.17 0.17 0.16
δCe 0.86 1.03 1.04 0.87 0.84 1.02 0.92 0.92 0.91 0.91 0.92 0.92 0.96 0.97 1.05 0.97 1.04 1.05 0.99
Rb 164 104 98.14 109 62.77 112 185 179 197 168 183 168 184 201 198 213 193 210 198
Ba 1,785 1,203 1,170 1,710 953 1,258 780 780 640 660 790 770 141 141 124 123 132 123 125
Th 8.28 10.84 10.60 15.08 11.94 10.13 24.30 32.70 16.90 21.40 25.00 19.75 20.31 22.14 19.49 18.28 19.92 20.88 21.26
U 1.63 2.22 2.06 3.01 2.20 2.04 1.70 2.30 1.60 1.40 1.90 1.40 2.85 3.53 3.20 2.92 3.54 3.04 3.03
Ta 0.51 0.32 0.38 0.40 0.28 0.34 1.45 1.41 2.46 1.24 1.30 0.94 1.27 1.43 1.18 1.23 1.21 1.23 1.43
Nb 9.90 7.37 8.59 9.38 7.22 8.00 14.90 13.70 13.60 10.50 12.90 12.00 20.65 21.76 18.21 18.66 19.14 17.92 21.18
Sr 2,355 3,016 3,162 3,305 4,703 3,004 228 267 268 260 252 237 30.82 33.33 27.30 23.06 34.73 21.19 27.60
P 6,940 5,939 7,132 6,672 7,951 6,879 611 480 742 436 393 436 226 122 42.74 104 80.76 153 225
Zr 205 232 227 350 210 219 98.20 93.40 79.40 72.30 88.40 88.70 273 287 312.56 248 235 205 203
Hf 5.16 5.37 5.32 6.25 4.86 5.33 3.70 3.60 3.00 2.70 3.40 3.40 7.45 8.04 8.11 7.74 7.50 7.23 7.17
Y 24.29 23.57 27.19 25.63 24.40 24.17 15.70 17.30 14.20 12.20 15.60 12.20 56.24 62.74 54.24 51.41 51.97 49.47 54.10

5.2.1 Huoersen gabbro

The samples of Huoersen gabbro have low-to-moderate LOL (1.32–1.83%). They show high CaO (9.9–12.7 wt%), MgO (7.0–8.6 wt%), and TiO2 (1.8–2.0 wt%), low SiO2 (45.7–48.3 wt%), Al2O3 (14.4–16.5 wt%), and K2O (1.2–2.0 wt%) contents, and relatively high Na2O (3.4–4.5 wt%), with low K2O/Na2O ratios (0.3–0.6). In the TAS diagram (Figure 5a), samples are plotted into in the field of monzogabbro. In the SiO2-K2O diagram (Figure 5b), most samples plot into the shoshonitic series.

Figure 5 (a) Total alkali vs silica diagram [72], (b) K2O vs SiO2 diagram [73], and c A/NK vs A/CNK diagram [74].
Figure 5

(a) Total alkali vs silica diagram [72], (b) K2O vs SiO2 diagram [73], and c A/NK vs A/CNK diagram [74].

The samples of Huoersen gabbro have high rare earth element (REE) (435–535 ppm). In the chondrite normalized REE diagram (Figure 6a), samples show higher light REE (LREE) and relatively lower heavy REE (HREE), with (La/Yb)N ratios of 32.81–51.63. In the primitive mantle-normalized spider diagram (Figure 6b), the samples exhibit enrichments in LILEs (e.g., Rb, Sr, Ba), weakly enrichments in Zr-Hf, and depletions in HFSEs (e.g., Nb, Ta, Ti).

Figure 6 Chondrite-normalized REE patterns and primitive-mantle-normalized trace element variation diagrams. The data for chondrite and primitive mantle are from [75]. (a and b) Huoersen gabbro. (c and d) Zongnaishan granite. (e and f) Huoersen granite.
Figure 6

Chondrite-normalized REE patterns and primitive-mantle-normalized trace element variation diagrams. The data for chondrite and primitive mantle are from [75]. (a and b) Huoersen gabbro. (c and d) Zongnaishan granite. (e and f) Huoersen granite.

5.2.2 Zongnaishan granite

The samples of Zongnaishan granites have moderate SiO2 (67.3–69.9%), Al2O3 (15.7–16.2%), Na2O (3.8–4.0%), and K2O (4.4–4.7%) contents, and the ratios of K2O/Na2O are 1.1–1.2. The samples plot into the field of quartz monzonite in the TAS diagram (Figure 5a) and belong to the high-K calc-alkaline series in the K2O-SiO2 diagram (Figure 5b). The samples have low TiO2 (0.30–0.39 wt%), CaO (1.52–2.07 wt%), and MgO (0.54–0.61 wt%) contents, and Mg number [Mg# = Mg/(Mg + Fe2+)] values are 27–32. In the A/NK-A/CNK diagram (Figure 5c), the samples’ plot belongs to the peraluminous series.

The REE of samples varies from 144 to 329 ppm. In the chondrite normalized REE diagram (Figure 6c), the samples are characterized by moderate negative Eu anomaly with δEu values of 0.30–0.49. In the primitive mantle-normalized spider diagram (Figure 6d), the samples exhibit enrichments in Rb, Th, U, and K and depletions in Nb, Ta, Sr, P, and Ti.

5.2.3 Huoersen granite

The samples of Huoersen granite exhibit extreme high SiO2 (74.78-77.44 wt%) contents, low TiO2 (0.18–0.22 wt%), Al2O3 (11.61–12.35 wt%), MgO (0.13–0.22 wt%), P2O5 (0.01–0.05 wt%), and CaO (0.23–0.70 wt%) contents, with Mg# values ranging from 45 to 63. The Na2O and K2O contents of 3.46–4.04 wt% and 4.52–5.72 wt%, respectively. All samples spot fall in the granite field in the TAS diagram (Figure 5a) and belong to high K-cala alkaline and shoshonite series in the SiO2 vs K2O diagram (Figure 5b). In addition, they display characteristics of peralkaline series in the A/NK vs A/CNK diagram (Figure 5c).

These granite samples have high REE contents (230–280 ppm). In the chondrite-normalized REE diagrams (Figure 6e), the granite shows enriched LREE, with middle negative Eu anomalies (Eu/Eu* = 0.16−0.17). In the primitive mantle-normalized trace element diagrams (Figure 6f), all granites sample depletions in Ba, Nb, Ta, Sr, P, and Ti, and enrichments in Rb, Th, U, P, K, and Pb.

5.3 Whole-rock Sr-Nd-Hf isotopic

Whole-rock Sm-Nd and Lu-Hf isotopic data for the Huoersen gabbro and granite in the Alxa region are given in Table 3. Whole-rock Rb-Sr and Sm-Nd isotopic data for the Zongnaishan granite in the Alxa region are given in Table 4. The initial 87Sr/86Sr, 143Nd/144Nd, 176Hf/177Hf, and ε Nd(t) and ε Hf(t) values were calculated by using the ages of zircon U-Pb for all samples.

Table 3

Whole-rock Nd-Hf isotopic data for the Huoersen gabbro and granite

Sample 147Sm/144Nd 143Nd/144Nd (143Nd/144Nd)i 2σ(10−6) ε Nd(t) T 2DM(Ma) 176Lu/177Hf 176Hf/177Hf (176Hf/177Hf)i 2σ(10−6) ε Hf(t) T 2DM(Ma)
Huoersen gabbro
16HE-2 0.099240 0.512570 0.512383 2 2.30 869 0.007096 0.282885 0.282847 4 9.00 733
16HE-3 0.099280 0.512568 0.512380 2 2.20 873 0.006397 0.282903 0.282868 5 9.80 685
16HE-4 0.100390 0.512562 0.512372 2 2.10 887 0.007399 0.282904 0.282864 3 9.60 694
16HE-6 0.095360 0.512560 0.512379 3 2.20 875 0.006527 0.282931 0.282896 5 10.70 622
Huoersen granite
16HE-7 0.122757 0.512587 0.512379 2 1.45 912 0.016063 0.282889 0.282811 4 7.08 832
16HE-8 0.123930 0.512588 0.512378 2 1.43 914 0.017154 0.282896 0.282813 3 7.14 828
16HE-9 0.125140 0.512579 0.512367 2 1.22 931 0.014805 0.282886 0.282814 3 7.19 825
16HE-10 0.125061 0.512583 0.512371 2 1.30 925 0.014609 0.282900 0.282829 3 7.72 791
Table 4

Whole-rock Sr-Nd isotopic data for the Zongnaishan granite

Sample 87Rb/86Sr 87Sr/86Sr (87Sr/86Sr)i 147Sm/144Nd 143Nd/144Nd Ɛ Nd(t) f Sm/Nd T 2DM(Ga)
Zongnaishan granite
16ZN-1 2.35 0.717305 0.708414 0.1179 0.512209 −0.58 −0.40 1.49
16ZN-2 1.941 0.715295 0.707949 0.1120 0.512193 −0.58 −0.43 1.43
16ZN-3 2.134 0.715809 0.707734 0.1236 0.512214 −0.58 −0.37 1.58
16ZN-4 1.871 0.714963 0.707883 0.1245 0.512241 −0.53 −0.37 1.55
16ZN-5 2.109 0.715506 0.707527 0.1141 0.512207 −0.56 −0.42 1.44
16ZN-6 2.059 0.716124 0.708333 0.1166 0.512191 −0.6 −0.41 1.50

5.3.1 Huoersen gabbro

The samples from Huoersen gabbro have initial 143Nd/144Nd ratios of 0.512372–0.512383 and positive ε Nd(t = 285 Ma) values of +2.1 to +2.3. They show high initial 176Hf/177Hf values of 0.282847–0.282896 and positive ε Hf(t) values of +9.0 to +10.7, yielding two-stage Hf model ages of 832–791 Ma.

5.3.2 Zongnaishan granite

The Zongnaishan gabbro have low initial 87Sr/86Sr values of 0.707527–0.708414. They show initial 143Nd/144Nd values of 0.512191–0.510041 and negative ε Nd(t) values of −0.37 to −0.43, yielding two-stage Nd model ages of 1.58–1.43 Ga.

5.3.3 Huoersen granite

The Huoersen granites have 143Nd/144Nd ratios of 0.512579–0.512588 and 176Hf/177Hf ratios of 0.282886–0.282900. Their initial 143Nd/144Nd and 176Hf/177Hf values vary from 0.512366 to 0.512378, 0.282811 to 20.282900, respectively, and positive ε Nd(t) values of +1.2 to +1.5 and ε Hf(t) values of +7.1 to +7.7, yielding two-stage Hf model ages of 733–622 Ma.

6 Discussion

6.1 Petrogenesis

6.1.1 Huoersen gabbro

The samples from Huoersen gabbro exhibit high MgO (6.96–8.62 wt%) contents, and varied greatly Mg# values (45–63) lower than values of primary magma (68–75) [46]. The contents of Cr (26–198 ppm) and Ni (169–223 ppm) varied widely, mean the parent magma of sample underwent fractional crystallization of olivine and pyroxene. In addition, the samples display slightly negative Eu anomalies (Figure 6a) and enrichment in Sr, suggesting that the fractional crystallization of plagioclase is weak.

The calc-alkaline Huoersen gabbro shows the characteristics of the island arc in the primitive-mantle-normalized trace element variation diagrams (Figure 6b), such as depleted in HFSEs (e.g., Nb, Ta, Ti) and enrichments in LREE and LILEs [47,48]. Remarkably, the Nb-Ta depletion could be induced by the crustal contamination of the basic magma [49]. But there is no clear contaminate signal of crustal materials for the samples from Huoersen gabbro: (a) the sample displays weakly negative Zr-Hf anomalies (Figure 6b), (b) their U/Nb ratios are very steady and not positively correlated with SiO2 contents (Figure 7), and (c) the Lu/Y (0.01), Nb/La (0.08), and Nb/Ce (0.04) are much lower than the range of continental crust values (Lu/Y of 0.16–0.18, Nb/La of 0.69, and Nb/Ce of 0.33) [50]. Furthermore, the subduction metasomatic fluids could also result in the Nb-Ta depletion, and the southern Alxa region was at a subduction of PAO tectonic setting during the early Permian [10,64,22,25]. In summary, the magmatic composition of Huoersen gabbro had not been significantly affected by crustal material involvement.

Figure 7 U/Nb vs SiO2 diagram of the Huoersen gabbro.
Figure 7

U/Nb vs SiO2 diagram of the Huoersen gabbro.

The samples from Huoersen gabbro have high La/Nb ratios (10.4–17.4), indicating that their magma sources were the product of lithospheric mantle (La/Nb ratios greater than 1.5), rather than asthenosphere mantle (La/Nb ratios less than 1.5) [51]. In addition, the sample has the geochemical characteristics of arc magma, reflecting the magmatic source that may be modified by subduction metasomatic fluids. The results are different from the magma of MORB (mid-ocean ridge basalt) or OIB (ocean island basalt) subjected to crustal contamination. However, the Nd-Hf isotopic systematics of Huoersen gabbro indicate that their sources are depleted mantle, which exhibit positive ε Nd(t) (+2.1 to +2.3) and ε Hf(t) values (+7.1 to +7.7). These decoupling characteristics of isotope and trace element are due to the metasomatism of subduction plates in the mantle source, resulting in enrichment in incompatible elements, such as K, Ba, and Sr [52]. Numerous studies have concluded that the southern CAOB occurred multistage subduction of oceanic plates during the Paleozoic [10,19,23,29,35,38]. So, the metasomatic components of the mantle source of the Huoersen gabbro parent magma are derived from the fluid released by the subduction slabs during the subduction of the PAO.

In conclusion, the Huoersen gabbro is the product of the depleted mantle metasomatized by subduction fluids.

6.1.2 Zongnaishan granite

Granites are important components in the continents and also closely related to collisional orogenic belt [53], which can be grouped into I-, S-, M-, and A-type granites based on their geochemical characteristics and tectonic setting [54,55,56,57,58]. The samples from Zongnaishan granite have moderate SiO2 (67.3–69.8 wt%) and Al2O3 contents (15.7–16.2 wt%). Their A/CNK values (1.05–1.14) are not exactly correspond with the characteristics of S-type granites (A/CNK value greater than 1.1) [58], and no aluminum-rich minerals (leucite, cordierite, etc.) are found in the mineral composition, so they do not belong to S-type granites. The samples have low (Zr + Nb + Ce + Y) values (154–264 ppm) and 10000Ga/Al ratios of 2.58–2.86. These are not completely consistent with the high SiO2, (Zr + Nb + Ce + Y) value (greater than 350 ppm) and 10,000 Ga/Al ratios (greater than 2.6) of A-type granites [57]. All samples plot into the OTG (unfractionated I- and S-type granites) field in the (Zr + Nb + Ce + Y) − (NaO2 + K2O)/CaO diagram (Figure 8). Therefore, the Zongnaishan granite is in agreement with I-type granites.

Figure 8 (Na2O + K2O)/CaO vs Zr + Nb + Ce + Y diagrams of the granite [54]. FG = fractionated felsic granites; OGT = unfractionated I- and S-type granites; A = A-type granite.
Figure 8

(Na2O + K2O)/CaO vs Zr + Nb + Ce + Y diagrams of the granite [54]. FG = fractionated felsic granites; OGT = unfractionated I- and S-type granites; A = A-type granite.

The Zongnaishan granites show depleted in HFSEs (e.g., Nb, Ta, Zr, and Ti), and enrichment in LILEs (e.g., Rb and Th), indicating that the magma source is dominated by components of continental crust. The samples’ enrichment in K and depletion of P also reflect the magma derived from crust. Moreover, the samples from Zongnaishan have initial 87Sr/86Sr values of 0.707527–0.708414, and negative ε Nd(t) values (−0.37 to −0.43) and two-stage Nd model ages of 1.58–1.43 Ga, suggesting that the Zongnaoshan granite is the product of remelting Neoproterozoic crust.

6.1.3 Huoersen granite

The samples from Huoersen granite have high SiO2, K2O, and Na2O contents, low MgO and CaO contents, enrichment in Rb, Th, U, Zr, and Hf, and depleted in Ba, Sr, Ti, Nb, and Ta, with 10,000 Ga/Al ratios of 4.2 (Zr + Nb + Ce + Y), values of 375–486 ppm, and are peralkaline (Figure 4a, A/CNK < 1), similar to that of A-type granites [54,56,57]. Moreover, all samples spot into the field of A-type granites in the (Zr + Nb + Ce + Y) − (NaO2 + K2O)/CaO diagram (Figure 8). Therefore, the Huoersen granite belongs to A-type granites.

Previous studies proposed various petrogenetic models for A-type granites: (a) fractional crystallization of mantle basaltic magma [59]; (b) partial melting of lower crustal material [57]; and (c) mixing of mantle magmas with crustal material [60]. It is usually accompanied by lots of mafic-ultramafic magmatism if A-type granite is derived from the crystallization differentiation of partially melted basalt magma [60], such as alkali granites in the western CAOB [53,61]. But there are no additional mafic magmas in the Alxa area. The sample has positive ε Nd(t) (+1.2 to +1.5) and ε Hf(t) values (+7.1 to +7.7), and T 2DM of 832–791 Ma, indicating the input of mantle material into crust. Because the femic constituents (MgO, Fe2O3 T) are low and because no mafic enclave was found in the sample rock, this could suggest that the mantle material was less during the magmatism process. This is obviously different from the granites of crust-mantle mixed, such as the granites of crust-mantle mixed are found in Hainan Island, China, and their most important feature was that they contain a large number of mafic enclaves [62]. The Nd/Th ratios (2.1–2.5) for Huoersen granite are close to the crustal source (3) [46], indicating that Huoersen granites are mainly the products of partial melting of the lower crust. So, the magma was derived from underplating resulting in partial melting of Neoproterozoic lower crust. The Huoersen granites have a low content of Sr and negative Eu anomalies (Figure 6e) showing the fractional crystallization of plagioclase during the process of magmatic evolution.

6.2 Tectonic implications

The ophiolite belts and intermediate‐acidic intrusive rock in the Alxa region record a complete Paleozoic tectonic history correlated with subduction and closing of PAO. [10,19,20,22,25,27,35,37,39,63]. The ca. 300 Ma Enger Us ophiolitic mélange along the Enger Us fault belt is the oldest ophiolitic in the Alxa region and is considered the final closure site of the PAO [33,34]. The Zongnaishan-Shalazhashan tectonic zone in the south of the Enger Us fault is the product of the island arc magmatic caused by the south subduction of the PAO during the early Paleozoic, and the ca. 275 Ma Quagan Qulu ophiolitic mélange is the residual body of the back-arc basin [10,64].

In this article, the geochemical data of Huoersen gabbro (ca. 285 Ma) show enrichment of LILEs and depletion of HFSEs, indicating a tectonic setting that may directly connected with island arcs. The preceding petrogenetic analysis also supports that the gabbro originated from partial melting of lithosphere mantle that was modified by subduction metasomatic fluids. Moreover, in the Hf/3-Th-Ta and Y/15-La/10-Nb/8 diagrams (Figure 9a and b), all samples were plotted into the island arc basalt and calc-alkaline arc basalt zone. Further, the Huoersen gabbro formed in the tectonic setting of the continental marginal arc, rather than interoceanic arc. The evidences are as follows: (a) interoceanic arc is most likely to occur in the initial stage of slab subduction, and the PAO was already in the late stage of subduction during early Permian in the Alxa region [10,20,30] and (b) they display a trend of continental marginal arc in the Ce-Yb diagram (Figure 9c). The Enger Us (ca. 300 Ma) and Quagan Qulu (Ca. 275 Ma) ophiolitic mélanges sporadically outcrop along two faults in the Alxa region (Figure 1c), considered a late Paleozoic ocean-arc system [34], which only implies that the PAO did not completely disappear prior to early Permian [10,22]. Researchers have proved that ca. 281 Ma Nuergai granitoids were occurred in a subduction setting [10]. So, there was subduction of ocean in the southern Alxa region during early Permian [27]. In conclusion, the studied Huoersen gabbro was related to this subduction which was sourced from lithospheric mantle metasomatized by subduction fluids.

Figure 9 Trace element discrimination diagrams for the tectonic setting of the Huoersen gabbro. (a) Hf/3-Th-Ta diagram [76]. (b) Y/15-La/10-Nb/8 diagram [77]. (c) Ce-Yb diagram [78]. CAB – continental margin arc basalt, IAB – island arc basalt, BAB – back arc basin basalt, N-MORB – normal mid-ocean ridge basalt, E-MORB – enriched mid-ocean ridge basalt, IAT – island arc tholeiite, WPT – within-plate tholeiite, WPAB – within-plate alkali basalt, 1A – calc-alkali basalt, 1B – transition region, 1C – ocean island tholeiite, 2A – Continental basalt, 3A – alkali basalt.
Figure 9

Trace element discrimination diagrams for the tectonic setting of the Huoersen gabbro. (a) Hf/3-Th-Ta diagram [76]. (b) Y/15-La/10-Nb/8 diagram [77]. (c) Ce-Yb diagram [78]. CAB – continental margin arc basalt, IAB – island arc basalt, BAB – back arc basin basalt, N-MORB – normal mid-ocean ridge basalt, E-MORB – enriched mid-ocean ridge basalt, IAT – island arc tholeiite, WPT – within-plate tholeiite, WPAB – within-plate alkali basalt, 1A – calc-alkali basalt, 1B – transition region, 1C – ocean island tholeiite, 2A – Continental basalt, 3A – alkali basalt.

The Zongnaishan granite (ca. 267 Ma) belongs to I-type granite, and all samples plot in the field of volcanic arc and syn-collisional granites in the Rb-Y + Nb and Nb + Y diagram (Figure 10). Its significant depletion of Nb-Ta and enrichment of LILEs (e.g., Rb, Cs, Sr, Ba) (Figure 6c) also support that they were formed in subduction environments. Geochemically, the Zongnaishan granites (A/CNK ratios of 1.01–1.13) have peraluminous characteristics of syn-collision magma and the significantly distinct low Ga/Al ratios (2.58–2.86) from the characteristic of intraplate extension setting [65] More importantly, numerous researches have suggested that the continental collision of southern Alxa region terminated at 268 Ma [10] (and references therein). Therefore, it can be concluded that Zongnaishan granites were generated in a syn-collision regime formed during the Zhusileng-Hangwula - Zongnaishan-Shalazhashan collision.

Figure 10 Tectonic environment discrimination diagrams of granite in the studied area. (a) Rb-Y + Nb diagram [79] and (b) Nb-Y diagram [79]. Syn-COLG – syn collisional granite, VAG – volcanic arc granite, WPG – within plate granite, POG – post-orogenic granite, ORG – oceanic ridge granite.
Figure 10

Tectonic environment discrimination diagrams of granite in the studied area. (a) Rb-Y + Nb diagram [79] and (b) Nb-Y diagram [79]. Syn-COLG – syn collisional granite, VAG – volcanic arc granite, WPG – within plate granite, POG – post-orogenic granite, ORG – oceanic ridge granite.

Eby [56] divided A-type granites into A1 and A2 subtypes. A1-subtype granite source is dominated by mantle and located in intraplate or continental rift environment, while A2-subtype granite source is dominated by crust, which is related to post-collision extensional environment. The Huoersen granites (ca. 259 Ma) have high Y/Nb (2.5–2.9) and Yb/Ta (4.2–4.8) ratios, indicative of A2-type granites affinities [56]. Moreover, all are classified into within-plate granite in the Rb-Y + Nb and Nb-Y diagram (Figure 10). Spatially, there are lots of late Permian to early Triassic magmatic activities related to the closure of PAO and subsequently post-collision extension regime in the southern Alxa region [29,66,67]. The Huoersen granites were products of the post-collision extension setting formed after the closure of PAO.

In general, a compressional geodynamic setting shows isotopic excursion to more enriched compositions, and an extensional setting exhibits excursion to more juvenile isotopes [68,69,70]. In the southern Alxa region, gradually evolved isotope signatures were recorded in the magmatic rocks during the late Paleozoic (Figure 11). The late Carboniferous to early Permian magmatic rocks demonstrates decreasing ε Nd(t) values, suggesting compression produced by the subduction of the PAO [10]. In contrast, the middle Permian to early Triassic magmatic rocks exhibit an extensional setting implied by increasing ε Nd(t) values (Figure 11). Notably, in the transitional period of early to middle Permian (280–265 Ma), a marked shift with decentralized positive to negative ε Nd(t) values illustrates a mixed magma source, corresponding to a tectonic switch from subduction to post-collision due to the closure of the PAO [10].

Figure 11 Whole-rock ε Nd(t) values vs ages from late Carboniferous to early Triassic igneous rocks in the Alxa region. Data and arrow from [9] and the arrow indicate ε Nd(t) values trends from Late Paleozoic igneous rocks in the Alxa region.
Figure 11

Whole-rock ε Nd(t) values vs ages from late Carboniferous to early Triassic igneous rocks in the Alxa region. Data and arrow from [9] and the arrow indicate ε Nd(t) values trends from Late Paleozoic igneous rocks in the Alxa region.

Combined with dating results of zircon U-Pb chronology and geodynamic mechanism of the studied Huoersen and Zongnaishan plutons, this paper infer that tectonic evolution of the southern Alxa region during the early Permian to late Permian involved three stages (Figure 12): a) Subduction of ocean (branch ocean of PAO) stage during ca. 285 Ma, when the Enger Us ocean southward subduction to Zongnaishan-Shalazhashan and resulted the formation of Huoersen gabbro (Figure 12a); b) Syn-collision stage during ca. 267 Ma, which means the Enger Us ocean closed during the middle Permian and formed Zongnaishan granite (Figure 12b); c) Post-collisional extensional setting during ca. 259 Ma (Figure 12c), and the asthenosphere mantle was upwelled and underplated lower crust, finally Huoersen granite were formed. The conclusion is consistent with regional magmatic events in this period.

Figure 12 Simplified schematic model of the formation of Permian magmatic rocks in the southern Alxa region. (a) The Enger Us ocean southward subduction to Zongnaishan-Shalazhashan and resulted the formation of Huoersen gabbro. (b) Syn-collision stage, which means the Enger Us ocean closed and formed Zongnaishan granite. (c) Post-collisional extensional setting and formed Huoersen granite.
Figure 12

Simplified schematic model of the formation of Permian magmatic rocks in the southern Alxa region. (a) The Enger Us ocean southward subduction to Zongnaishan-Shalazhashan and resulted the formation of Huoersen gabbro. (b) Syn-collision stage, which means the Enger Us ocean closed and formed Zongnaishan granite. (c) Post-collisional extensional setting and formed Huoersen granite.

7 Conclusions

In this article, we present a petrographic, geochronological, whole-rock major and trace element, Sr-Nd-Hf isotopic data, Permian gabbro, and granite samples from the Alxa region. The major conclusions are as follows:

(1) The LA-ICP-MS zircon U-Pb age of Huoersen gabbro and granite, Zongnaishan granite, is ca. 285, 259 and 267 Ma, respectively.

(2) The calc-alkaline Huoersen gabbro is derived from the depleted mantle metasomatized by subduction fluids. The I-type Zongnaishan granite is the product of crustal remelting of Neoproterozoic. The A2-subtype Huoersen granites are the products of partial melting of the lower crust.

(3) Combined with previous studies, a model is proposed involving subduction (ca. 285 Ma), syn-collision (267 Ma), and post-collisional extension (ca. 259 Ma) for an oceanic branch of PAO in the Alxa region.

  1. Funding information: This study was supported by Fundamental Research Funds for the Central Universities (lzujbky-2023-it17), the China Atomic Energy Authority (CAEA) through the Geological Disposal Program, and the National Second Tibetan Plateau Expedition Program (2019QZKK0901).

  2. Author contributions: Conception, E.W., X.Z., and J.W.; methodology, E.W., X.Z., Y.H. R.S., Z.G., and C.L.; investigation, E.W., W.C., L.W., G.S., and Y.H.; data curation, E.W., W.C., L.W., G.S., and Z.G.; writing – original draft, E.W.; writing – review and editing, X.Z. and J.W.; project administration, X.Z. and J.W; and funding acquisition, E.W., X.Z., and J.W. All authors have read and agreed to the published version of the article.

  3. Conflict of interest: The authors declare that there is no conflict of interest.

  4. Data availability statement: Data available on request from the author.

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Received: 2023-09-19
Revised: 2023-12-18
Accepted: 2024-01-28
Published Online: 2024-03-16

© 2024 the author(s), published by De Gruyter

This work is licensed under the Creative Commons Attribution 4.0 International License.

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  66. Efficient development technology of Upper Paleozoic Lower Shihezi tight sandstone gas reservoir in northeastern Ordos Basin
  67. Assessment of soil resources of agricultural landscapes in Turkestan region of the Republic of Kazakhstan based on agrochemical indexes
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  69. Petrogenetic relationship between plutonic and subvolcanic rocks in the Jurassic Shuikoushan complex, South China
  70. A novel workflow for shale lithology identification – A case study in the Gulong Depression, Songliao Basin, China
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  76. Application of the wavelet transform and Hilbert–Huang transform in stratigraphic sequence division of Jurassic Shaximiao Formation in Southwest Sichuan Basin
  77. Structural detachment influences the shale gas preservation in the Wufeng-Longmaxi Formation, Northern Guizhou Province
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  87. Prediction of formation fracture pressure based on reinforcement learning and XGBoost
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  97. Formation mechanism and oil-bearing properties of gravity flow sand body of Chang 63 sub-member of Yanchang Formation in Huaqing area, Ordos Basin
  98. Diagenesis of marine-continental transitional shale from the Upper Permian Longtan Formation in southern Sichuan Basin, China
  99. Vertical high-velocity structures and seismic activity in western Shandong Rise, China: Case study inspired by double-difference seismic tomography
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  102. Research on spatial correlation structure of war heritage based on field theory. A case study of Jinzhai County, China
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  105. Deeply buried clastic rock diagenesis evolution mechanism of Dongdaohaizi sag in the center of Junggar fault basin, Northwest China
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  117. Predicting stability factors for rotational failures in earth slopes and embankments using artificial intelligence techniques
  118. Origin of Late Cretaceous A-type granitoids in South China: Response to the rollback and retreat of the Paleo-Pacific plate
  119. Modification of dolomitization on reservoir spaces in reef–shoal complex: A case study of Permian Changxing Formation, Sichuan Basin, SW China
  120. Geological characteristics of the Daduhe gold belt, western Sichuan, China: Implications for exploration
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  128. Characteristics and control techniques of soft rock tunnel lining cracks in high geo-stress environments: Case study of Wushaoling tunnel group
  129. Influence of pore structure characteristics on the Permian Shan-1 reservoir in Longdong, Southwest Ordos Basin, China
  130. Study on sedimentary model of Shanxi Formation – Lower Shihezi Formation in Da 17 well area of Daniudi gas field, Ordos Basin
  131. Multi-scenario territorial spatial simulation and dynamic changes: A case study of Jilin Province in China from 1985 to 2030
  132. Review Articles
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  137. Erratum
  138. Erratum to “Random forest and artificial neural network-based tsunami forests classification using data fusion of Sentinel-2 and Airbus Vision-1 satellites: A case study of Garhi Chandan, Pakistan”
  139. Special Issue: Natural Resources and Environmental Risks: Towards a Sustainable Future - Part I
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  143. Application of remote sensing in monitoring land degradation: A case study of Stanari municipality (Bosnia and Herzegovina)
  144. Optimizing agricultural land use: A GIS-based assessment of suitability in the Sana River Basin, Bosnia and Herzegovina
  145. Assessing risk-prone areas in the Kratovska Reka catchment (North Macedonia) by integrating advanced geospatial analytics and flash flood potential index
  146. Analysis of the intensity of erosive processes and state of vegetation cover in the zone of influence of the Kolubara Mining Basin
  147. GIS-based spatial modeling of landslide susceptibility using BWM-LSI: A case study – city of Smederevo (Serbia)
  148. Geospatial modeling of wildfire susceptibility on a national scale in Montenegro: A comparative evaluation of F-AHP and FR methodologies
  149. Geosite assessment as the first step for the development of canyoning activities in North Montenegro
  150. Urban geoheritage and degradation risk assessment of the Sokograd fortress (Sokobanja, Eastern Serbia)
  151. Multi-hazard modeling of erosion and landslide susceptibility at the national scale in the example of North Macedonia
  152. Understanding seismic hazard resilience in Montenegro: A qualitative analysis of community preparedness and response capabilities
  153. Forest soil CO2 emission in Quercus robur level II monitoring site
  154. Characterization of glomalin proteins in soil: A potential indicator of erosion intensity
  155. Power of Terroir: Case study of Grašac at the Fruška Gora wine region (North Serbia)
  156. Special Issue: Geospatial and Environmental Dynamics - Part I
  157. Qualitative insights into cultural heritage protection in Serbia: Addressing legal and institutional gaps for disaster risk resilience
https://doi.org/10.1515/geo-2022-0618
Keywords for this article
geochemical; Permian; tectonic switch; Alxa region; Central Asian Orogenic Belt
Creative Commons
BY 4.0

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  128. Characteristics and control techniques of soft rock tunnel lining cracks in high geo-stress environments: Case study of Wushaoling tunnel group
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  134. Prediction and assessment of meteorological drought in southwest China using long short-term memory model
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  139. Special Issue: Natural Resources and Environmental Risks: Towards a Sustainable Future - Part I
  140. Spatial-temporal and trend analysis of traffic accidents in AP Vojvodina (North Serbia)
  141. Exploring environmental awareness, knowledge, and safety: A comparative study among students in Montenegro and North Macedonia
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  143. Application of remote sensing in monitoring land degradation: A case study of Stanari municipality (Bosnia and Herzegovina)
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  146. Analysis of the intensity of erosive processes and state of vegetation cover in the zone of influence of the Kolubara Mining Basin
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  148. Geospatial modeling of wildfire susceptibility on a national scale in Montenegro: A comparative evaluation of F-AHP and FR methodologies
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  150. Urban geoheritage and degradation risk assessment of the Sokograd fortress (Sokobanja, Eastern Serbia)
  151. Multi-hazard modeling of erosion and landslide susceptibility at the national scale in the example of North Macedonia
  152. Understanding seismic hazard resilience in Montenegro: A qualitative analysis of community preparedness and response capabilities
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  155. Power of Terroir: Case study of Grašac at the Fruška Gora wine region (North Serbia)
  156. Special Issue: Geospatial and Environmental Dynamics - Part I
  157. Qualitative insights into cultural heritage protection in Serbia: Addressing legal and institutional gaps for disaster risk resilience
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