Startseite Geochronology and geochemistry of late Paleozoic volcanic rocks in eastern Inner Mongolia and their geological significance
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Geochronology and geochemistry of late Paleozoic volcanic rocks in eastern Inner Mongolia and their geological significance

  • Liang Tianyi , Li Mengmeng EMAIL logo , Wang Li , Wang Guanhong , Tang Xinglong und Li Zhuang
Veröffentlicht/Copyright: 7. April 2025
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Abstract

The Daxing’anling region in Inner Mongolia has always been the most active area of tectonic magmatic activity in the Xingmeng orogenic belt. This study investigated the rock geochemistry of trachyandesite and rhyolite tuff of the Late Carboniferous Gegen Aobao Formation in eastern Inner Mongolia. This study presents new petrography, zircon U-Pb age, and whole-rock geochemical data for the Late Carboniferous Gegenaobao Formation in volcanic rocks in order to constrain their petrogenesis and geodynamic setting. The results indicate that the aluminum content of trachyandesite is relatively high, and the calcium and magnesium content is higher than that of rhyolite tuff, showing a sodium-rich characteristic. It is a quasi-aluminum peraluminous rock, and the europium anomaly is not obvious. The formation age is 304.4 ± 2.3 Ma. The calcium and magnesium content of the rhyolite tuff is relatively low, exhibiting characteristics of calcium alkali and weak peraluminous rocks. It has more obvious characteristics of light and heavy rare earth fractionation and negative europium anomalies, with a formation age of 307.6 ± 2.0 Ma. Comprehensive analysis shows that the magma of Late Carboniferous volcanic rocks in eastern Inner Mongolia mainly originates from the crust, with a deeper source of andesite and partial melting of the mantle material. Both are tectonic environments of continental margin arc volcanic rocks. The Xing’an Block and the Songnen Block completed collision assembly in the Early Carboniferous and were in a post-orogenic extension environment in the Late Carboniferous. The ancient Asian Ocean in the northern part of the Erlian Hegenshan Zhalantun Heihe tectonic belt had already closed in the Late Carboniferous, and the Xingmeng orogenic belt began to enter the orogenic extension stage.

Keywords: U-Pb chronology; rock geochemistry; Xingmeng orogenic belt; magmatic genesis

1 Introduction

The Xingmeng orogenic belt in eastern Inner Mongolia is one of the most significant regions for continental accretion and mountain building between the two major plates [1]. The study of its tectonic evolution has always been a focus of attention for scholars both domestically and internationally [2]. According to the latest research, the Xingmeng orogenic belt completed the collision and collage of the Siberian and North China plates through the assembly of numerous microcontinents within the ancient Asian Ocean [3]. By studying the evolution of tectonic zones between numerous microplates, numerous theories on the evolution of the ancient Asian Ocean have gradually emerged [4,5]. The Erlian Hegenshan Heihe tectonic belt is an important tectonic belt in the Xingmeng region, located between the Xing’an and Songnen blocks. It is also considered one of the six major subduction zones in Inner Mongolia [6]. Some scholars initially believed that this tectonic zone was the final closure position of the ancient Asian Ocean, but others believed that it was only the collision closure position between the Xing’an Block and the Songnen Block [7,8,9] and did not represent the final position of the ancient Asian Ocean. At the same time, different views have been put forward on the formation time limit of this tectonic belt. Some scholars believe that the Xing’an and Songnen blocks completed collision and assembly during the Late Devonian Early Carboniferous [7,10–12]. Some scholars also believe that the Xing’an and Songnen blocks were still active during the Early Permian, and the magmatic activity in the Late Paleozoic was mainly caused by the subduction of oceanic crust [13]. In summary, further research is needed on the tectonic magmatic evolution of the Xingmeng orogenic belt in the late Paleozoic era.

The research area is located in the middle section of the Greater Khingan Range, with the Erenhot Hegenshan Heihe ophiolite belt passing through the southern part of the studied area. The Late Paleozoic volcanic rocks widely distributed in the study area are important research objects for studying the evolution of the Xingmeng orogenic belt. Through field systematic geological surveys and sampling work, systematic petrographic, zircon U-Pb geochronology, and geochemical analysis were conducted on the combination of intermediate to felsic volcanic rocks to explore their age, petrogenetic, and tectonic background. Further analysis was conducted on the combination process of the Late Paleozoic Xing’an Block and the Songnen Block in the middle section of the Greater Khingan Range, providing reliable basic data for studying the evolution of the Paleozoic Xingmeng orogenic belt and improving the research level of the tectonic magmatic evolution of the Xingmeng orogenic belt in the Late Paleozoic.

2 Geological overview

The research area is located at the contact point between the Xing’an block and the Songnen block. The regional geological structure is located on the Dongwuqi Duobaoshan island arc, and the Erenhot Hegenshan suture zone is located in the southern part of the working area (Figure 1a). The Paleozoic rocks are widely distributed in the research area, accompanied by a certain scale of Mesozoic volcanic rock strata and intrusive rocks. The Paleozoic strata are mainly composed of the Late Carboniferous Gegenaobao Formation (C2 g), which is a set of marine felsic volcanic lava/volcanic debris rock combinations. It is in angular unconformity contact with the overlying Linxi Formation (P3 l). The Linxi Formation (P3 l) is a set of marine land interaction facies clastic rock combinations, mainly composed of sandstone, siltstone, and interbedded limestone. The Mesozoic volcanic rocks are mainly the Manketou Ebo Formation (J3m) of the Jurassic system, which is composed of terrestrial felsic volcanic rocks, and the Baiyin Gaolao Formation (K1b) of the Cretaceous system, which is mainly composed of felsic volcanic rocks. The intrusive rocks are mainly of the Cretaceous period (Figure 1b and c).

Figure 1 Geologic map in the study area.
Figure 1

Geologic map in the study area.

The Carboniferous Gegen Aobao Formation is the main stratigraphic unit in the work area, which is widely spread. Through detailed field research and profile measurements, the lower part of this formation is found to be mainly composed of marine, terrestrial clastic rocks, including metamorphic quartz sandstone, feldspar sandstone, metamorphic siltstone, and mudstone slate, which have obvious metamorphic phenomena such as sericite and chloritization. The central region is mainly composed of intermediate volcanic rocks, including trachyandesite (including pores), trachyte, breccia lava, andesite tuff, and a small amount of felsic tuff. The upper part is mainly composed of felsic rocks such as rhyolite tuff, rhyolite, and a small amount of breccia lava.

Trachyandesite is mainly gray-brown in color, with a spotted structure and a spotted crystal content of 10%. It is mainly composed of plagioclase and a small amount of biotite, with a spotted grain size of 0.30–2.00 mm. The matrix is mainly composed of plagioclase and a small amount of opaque minerals. Plagioclase is mostly needle-shaped with a particle size of 0.02–0.06 mm. Rocks have a small amount of developed pores, which are mainly filled with epidote. It can be seen that the rock has undergone strong epidote and silicification, with developed fractures filled with iron and epidote (Figure 2a and c).

Figure 2 Field outcrop and microphotographs of volcanic rocks in the study area. Pl, Plagioclase; Qtz, quartz; and Kfs, K-feldspar.
Figure 2

Field outcrop and microphotographs of volcanic rocks in the study area. Pl, Plagioclase; Qtz, quartz; and Kfs, K-feldspar.

The color of rhyolite tuff is mainly gray, with a tuffaceous structure and blocky structure. Volcanic breccia is composed of tuff, which is angular or irregular in shape, with a gravel diameter of 2.00–15.00 mm and a content of about 8%. The main components of rock debris are tuff and andesite, which are subrounded or subangular in shape, with a particle size of 0.05–2.00 mm and a content of about 5%. The main components of crystal fragments are plagioclase, potassium feldspar, and a small amount of quartz, which are irregular in shape. The grain size of crystal fragments is 0.05–2.00 mm, and individual crystal fragments can reach 3.00 mm, with a content of about 35%. The glass shards are irregular in shape, with most of them undergoing devitrification. Some undergo slight polarization reactions, while others crystallize into small quartz crystals, accounting for about 52% (Figure 2b and d).

3 Materials and methods

This work mainly focuses on the study of trachyandesite and rhyolitic tuff in the volcanic rock suit of the Gegenaobao Formation, including petrology, chronology, and rock geochemistry. The zircon chronology samples are numbered trachyandesite (TW5) and rhyolitic tuff (TW16), and the rock geochemical samples are numbered trachyandesite (G1–G8) and rhyolitic tuff (H1–H7). The sampling locations are shown in Figure 1b.

Single mineral sorting was conducted at the Regional Geological Survey and Research Institute of Langfang City, Hebei Province. First, each sample is crushed to an appropriate particle size, cleaned, dried, and screened, and zircon crystals of different particle sizes are separated using magnetic and heavy liquid separation methods. CL image (cathodoluminescence image) shooting and LA-ICP-MS U-Pb dating were completed at Beijing Kehui Testing Technology Co., Ltd. The laser ablation inductively coupled plasma mass spectrometer was used (Jena Elite, Germany), and the laser model was Newwave 193-UC (USA). Based on the cathodoluminescence and transmission light images of zircon, suitable zircon positions without inclusions and cracks were selected [14]. A 193 mm excimer laser was used to etch the surface of the zircon, with a laser ablation diameter of 25 μm, and the erosion frequency is 10 Hz. Using He as a carrier for erosion material, transport the erosion material to a mass spectrometer for testing and analysis. The high-frequency transmitter power of ICPMS is 1200w, the cooling gas (Ar) flow is 9 L/min, and the material of the cone is nickel. The integration time for analysis is a total of 40 s, and the blank collection time is 30 s. The sample data were processed using NIST 610 and GJ-1 as internal zircon standards, and the software was analyzed and plotted using the ICPMSData program and the Isopolot program [15].

A total of 15 samples were analyzed for major and trace elements geochemistry. First, the samples were subjected to weathering shell removal and then crushed and ground into powder using a ball mill. The testing and analysis of major and trace elements were completed by the laboratory of the Hebei Provincial Institute of Regional Geological and Mineral Resources Survey. The major elements were tested using the Axios Max X-ray fluorescence spectrometer, with an accuracy better than 5%. Trace elements were tested using an inductively coupled plasma mass spectrometer, with an analysis accuracy better than 5%.

4 Analysis results

4.1 Zircon U–Pb geochronology

The results of zircon U–Pb isotope analysis in the study area are shown in Tables 1 and 2. The zircon U–Pb age harmony diagram and some zircon cathodoluminescence diagrams are shown in Figure 3. The selected zircon samples are mostly in the shape of long columns or squares with good transparency. The diameter of zircon particles is mostly between 100 and 200 μm. Zircons have distinct rhythmic bands of magmatic origin. According to previous research, the corresponding Th and U content and Th/U of zircons vary depending on their genesis [16,17]. Generally, magmatic zircons have Th/U greater than 0.4, while metamorphic zircons have lower Th and U content, with Th/U often less than 0.07 [18]. The Th/U of TW5 zircon sample ranges from 0.47 to 2.01, while the Th/U of TW16 ranges from 0.44 to 0.76, both of which are greater than 0.4, showing obvious magmatic zircon characteristics.

Table 1

LA-ICP-MS U–Pb isotope analysis results of zircon from trachyandesite (TW5) in the study area

Tested point Isotope ratios and errors Age and error (Ma/σ)
207Pb/206Pb 1σ 207Pb/235U 1σ 206Pb/238U 1σ 207Pb/206Pb 1σ 207Pb/235U 1σ 206Pb/238U 1σ
TW5-01 0.0515 0.0036 0.3382 0.0234 0.0483 0.0008 261.2 158.3 295.8 17.8 303.9 4.7
TW5-02 0.0540 0.0032 0.3618 0.0212 0.0491 0.0008 372.3 133.3 313.6 15.8 309.0 4.7
TW5-03 0.0545 0.0032 0.3589 0.0215 0.0476 0.0008 390.8 131.5 311.4 16.1 300.0 4.6
TW5-04 0.1085 0.0062 0.6200 0.0321 0.0424 0.0007 1775.9 99.1 489.9 20.2 267.6 4.6
TW5-05 0.0746 0.0095 0.2120 0.0274 0.0215 0.0006 1058.3 253.2 195.2 22.9 137.0 3.5
TW5-06 0.0575 0.0035 0.3889 0.0244 0.0488 0.0007 522.3 133.3 333.6 17.8 307.0 4.5
TW5-07 0.0563 0.0033 0.3739 0.0211 0.0483 0.0008 464.9 129.6 322.5 15.6 303.9 5.1
TW5-08 0.0506 0.0033 0.3368 0.0220 0.0482 0.0008 220.4 150.0 294.7 16.7 303.4 4.8
TW5-09 0.0537 0.0022 0.3563 0.0137 0.0483 0.0006 366.7 94.4 309.4 10.3 304.0 4.0
TW5-10 0.0562 0.0026 0.3672 0.0158 0.0478 0.0007 461.2 103.7 317.6 11.7 301.1 4.3
TW5-11 0.0853 0.0043 0.5544 0.0248 0.0478 0.0007 1324.1 97.8 447.9 16.2 301.1 4.5
TW5-12 0.0598 0.0044 0.3961 0.0288 0.0482 0.0008 598.2 159.2 338.8 20.9 303.2 4.6
TW5-13 0.0594 0.0039 0.3852 0.0246 0.0477 0.0008 581.2 143.3 330.8 18.0 300.2 4.7
TW5-14 0.0531 0.0029 0.1589 0.0084 0.0218 0.0003 331.5 121.3 149.7 7.4 139.3 2.0
TW5-15 0.0495 0.0030 0.3268 0.0193 0.0481 0.0006 172.3 137.9 287.2 14.8 302.9 3.9
TW5-16 0.0650 0.0036 0.4136 0.0195 0.0469 0.0007 772.2 116.7 351.5 14.0 295.6 4.5
TW5-17 0.0561 0.0033 0.3795 0.0219 0.0491 0.0007 457.5 132.4 326.7 16.1 308.8 4.3
TW5-18 0.0500 0.0038 0.3422 0.0259 0.0501 0.0009 198.2 177.8 298.8 19.6 314.9 5.3
TW5-19 0.0599 0.0031 0.3985 0.0203 0.0485 0.0006 598.2 112.9 340.6 14.7 305.3 3.9
TW5-20 0.0485 0.0035 0.3276 0.0235 0.0483 0.0009 124.2 159.2 287.8 18.0 304.1 5.2
Table 2

Zircon LA-ICP-MS U-Pb data for Rhyolitic tuff (TW16) in the study area

Tested point Isotope ratios and errors Age and error (Ma/σ)
207Pb/206Pb 1σ 207Pb/235U 1σ 206Pb/238U 1σ 207Pb/206Pb 1σ 207Pb/235U 1σ 206Pb/238U 1σ
TW16-01 0.0599 0.0036 0.4005 0.0237 0.0484 0.0007 611.1 123.1 342.0 17.2 304.5 4.3
TW16-02 0.0605 0.0031 0.3975 0.0194 0.0481 0.0006 633.4 109.2 339.9 14.1 302.9 4.0
TW16-03 0.0529 0.0026 0.3560 0.0167 0.0492 0.0006 324.1 113.0 309.3 12.5 309.5 3.8
TW16-04 0.0523 0.0030 0.3510 0.0198 0.0491 0.0006 298.2 133.3 305.5 14.9 308.9 3.6
TW16-05 0.0535 0.0038 0.3510 0.0234 0.0488 0.0007 350.1 156.5 305.5 17.6 307.4 4.4
TW16-06 0.0531 0.0026 0.3533 0.0169 0.0486 0.0006 344.5 111.1 307.2 12.7 306.2 3.8
TW16-07 0.0522 0.0029 0.3517 0.0198 0.0487 0.0006 300.1 125.9 306.0 14.9 306.6 3.8
TW16-08 0.0570 0.0026 0.3855 0.0172 0.0494 0.0006 500.0 101.8 331.1 12.6 310.7 3.8
TW16-09 0.0552 0.0027 0.3678 0.0172 0.0485 0.0006 420.4 107.4 318.0 12.8 305.5 3.8
TW16-10 0.0506 0.0036 0.3401 0.0250 0.0487 0.0010 220.4 166.6 297.3 18.9 306.6 5.9
TW16-12 0.0524 0.0036 0.3542 0.0241 0.0494 0.0011 301.9 157.4 307.9 18.1 310.8 6.6
TW16-13 0.0576 0.0030 0.3837 0.0192 0.0488 0.0007 522.3 119.4 329.7 14.1 307.1 4.6
TW16-14 0.0493 0.0025 0.3337 0.0166 0.0491 0.0007 164.9 116.7 292.4 12.7 309.0 4.3
TW16-15 0.0484 0.0035 0.3226 0.0212 0.0488 0.0008 120.5 159.2 283.9 16.3 307.0 4.9
TW16-16 0.0517 0.0053 0.3420 0.0329 0.0493 0.0011 333.4 233.3 298.7 24.9 310.0 6.9
TW16-17 0.0523 0.0024 0.3525 0.0153 0.0493 0.0007 298.2 103.7 306.6 11.5 310.0 4.4
TW16-18 0.0536 0.0035 0.3599 0.0217 0.0492 0.0007 353.8 148.1 312.2 16.2 309.4 4.5
TW16-19 0.0512 0.0029 0.3400 0.0189 0.0487 0.0008 250.1 126.8 297.2 14.3 306.6 4.6
TW16-20 0.0484 0.0040 0.3281 0.0278 0.0492 0.0012 116.8 185.2 288.1 21.2 309.8 7.1
Figure 3 Zircon U–Pb age harmony map and partial zircon cathodoluminescence (CL) map of trachyandesite (TW5) and rhyolite tuff (TW16) in the study area.
Figure 3

Zircon U–Pb age harmony map and partial zircon cathodoluminescence (CL) map of trachyandesite (TW5) and rhyolite tuff (TW16) in the study area.

A total of 20 zircon measurement spots were obtained from the trachyandesite (TW5) sample. On the 206Pb/238U-207Pb/235U harmonic map, the measurement points TW5-04, TW5-05, and TW5-14 have poor harmony, so they were not included in the final calculation. The weighted mean age of the remaining measurement points is 304.4 ± 2.3 Ma, with MSWD = 0.63, which represents the age of the formation of trachyandesite. A total of 19 zircon measurement points were obtained from the rhyolitic tuff (TW16) sample, which was shown on the 206Pb/238U-207Pb/235U harmonic map. All 19 measurement points were included in the projection calculation, with an age-weighted average of 307.6 ± 2.0 Ma and MSWD = 0.25, which represents the age of the formation of rhyolite tuff.

4.2 Geochemistry

4.2.1 Major element characteristics

The main elemental analysis results of trachyandesite are shown in Table 3. The SiO2 content ranges from 55.40 to 58.02%, with a high Al2O3 content of 14.89–19.29%, MgO content of 1.52–3.26%, CaO content of 3.33–7.57%, P2O5 content of 0.24–0.52%, total alkali (ALK) content of 4.41–7.64%, and a mean of 6.36%. The rocks exhibit sodium-rich characteristics, with Na2O content of 3.19–5.20%, an aluminum saturation index (A/CNK) of 0.83–1.05, and a Rittman index (σ) of 0.83–1.05, ranging from 1.42 to 3.71, with an average of 2.82, exhibiting calc-alkaline characteristics. The Mg# value ranges from 30.23 to 49.53, with an average of 41.98. According to the TAS diagram of volcanic rocks (Figure 4), most of the samples fall within the range of trachyandesite, with two samples falling within the range of andesite. According to the SiO2–K2O diagram (Figure 5), the samples are mostly calcium-alkaline (high potassium) series rocks, with one sample located within the range of potassium basalt. Due to the complex genesis and diversity of volcanic rocks, they may form rock types with subtle differences due to different geological environments and magmatic processes. According to the A/CNK–A/NK diagram (Figure 6), it is shown that the trachyandesite has semialuminous to peraluminous characteristics.

Table 3

Analysis results of major elements (%) and trace elements (ppm) in coarse Anite in the study area

Sample number G1 G2 G3 G4 G5 G6 G7 G8
Lithology Trachy-andesite Trachy-andesite Andesite Trachy-andesite Trachy-andesite Trachy-andesite Andesite Trachy-andesite
SiO2 57.62 55.58 55.40 58.02 56.72 56.70 56.42 55.42
TiO2 0.86 0.90 1.17 1.60 1.45 1.01 1.55 0.97
Al2O3 18.30 19.29 18.17 14.89 16.71 16.23 14.92 16.25
Fe2O3 3.33 3.43 2.36 4.45 4.89 3.33 3.64 3.47
FeO 3.63 3.66 4.13 3.92 2.19 2.87 4.20 2.80
MnO 0.11 0.11 0.27 0.12 0.12 0.15 0.11 0.13
MgO 3.18 3.18 1.52 2.61 2.89 2.58 2.74 3.26
CaO 4.51 5.03 7.57 3.33 4.58 3.59 5.40 4.28
Na2O 5.00 5.10 3.55 5.20 4.56 3.19 3.78 5.14
K2O 1.28 1.36 0.86 2.44 2.25 3.37 1.71 2.09
P2O5 0.24 0.26 0.37 0.44 0.52 0.29 0.41 0.28
LOI 1.17 1.02 4.00 2.32 2.40 6.02 4.43 5.59
TOTAL 99.23 98.92 99.37 99.32 99.31 99.32 99.32 99.69
ALK 6.28 6.46 4.41 7.64 6.81 6.56 5.49 7.23
Na2O/K2O 3.91 3.75 4.13 2.13 2.03 0.95 2.21 2.46
A/CNK 1.03 1.02 0.89 0.86 0.92 1.05 0.83 0.88
DI 59.49 56.83 50.43 68.92 62.10 64.66 58.22 63.77
σ 2.61 3.16 1.42 3.68 3.17 2.77 2.03 3.71
SI 19.39 19.04 12.25 14.06 17.40 16.88 17.05 19.53
Mg# 46.10 45.66 30.23 36.99 43.87 43.94 39.52 49.53
V 74.20 83.77 159.13 244.04 181.86 125.48 225.46 144.19
Cr 9.40 4.72 2.24 6.94 14.32 6.17 14.52 5.31
Ni 3.71 5.36 3.82 9.62 13.46 5.86 11.84 5.80
Ga 22.34 19.10 21.04 22.73 23.18 21.92 22.20 19.30
Rb 38.66 34.69 17.26 47.55 40.35 83.65 36.05 55.51
Sr 558.96 475.58 1028.39 714.10 1018.49 578.32 637.26 559.11
Zr 226.02 174.50 161.54 232.00 220.08 181.42 208.17 154.40
Nb 7.67 8.01 6.14 9.10 11.64 7.82 8.61 6.75
Ba 834.27 579.98 650.88 820.80 901.32 1700.93 937.14 621.23
Hf 5.85 4.70 4.66 6.60 5.78 5.22 6.11 4.68
Ta 0.42 0.38 0.36 0.58 0.62 0.51 0.48 0.45
W 0.03 0.44 0.26 0.37 0.45 0.43 0.35 0.26
Pb 17.31 11.74 12.18 15.43 14.74 15.77 12.92 11.53
Th 3.11 2.48 2.78 4.28 3.68 4.13 3.99 3.43
U 0.72 0.60 0.68 1.17 1.11 1.29 1.11 0.83
La 25.40 19.70 22.00 27.80 33.50 25.20 24.90 21.60
Ce 43.40 44.40 45.00 59.50 68.00 48.50 51.70 41.00
Pr 5.81 4.57 6.08 7.97 8.96 6.61 7.10 5.47
Nd 24.10 19.00 26.50 33.80 36.10 27.80 31.50 23.20
Sm 4.76 3.85 5.23 7.03 7.10 5.44 6.35 4.73
Eu 1.46 1.15 1.67 1.96 2.10 1.92 1.71 1.47
Gd 3.84 3.07 4.39 5.80 5.77 4.76 5.21 4.01
Tb 0.60 0.48 0.67 0.88 0.80 0.71 0.78 0.61
Dy 3.46 2.79 3.55 4.92 4.15 3.78 4.25 3.34
Ho 0.64 0.51 0.61 0.89 0.71 0.68 0.78 0.62
Er 1.70 1.40 1.73 2.40 1.94 1.91 2.11 1.77
Tm 0.26 0.22 0.29 0.39 0.33 0.31 0.37 0.30
Yb 1.58 1.32 1.65 2.34 1.89 1.82 2.11 1.74
Lu 0.25 0.22 0.25 0.36 0.28 0.29 0.32 0.27
Y 19.90 15.80 18.00 24.40 22.50 20.90 21.60 17.10
ΣREE 117.26 102.68 119.62 156.04 171.63 129.73 139.19 110.13
LaN/YbN 11.53 10.71 9.56 8.52 12.71 9.93 8.46 8.90
δEu 1.04 1.02 1.07 0.94 1.00 1.15 0.91 1.03
δCe 0.88 1.15 0.95 0.98 0.96 0.92 0.95 0.92
Figure 4 TAS diagram of volcanic rocks in the study area.
Figure 4

TAS diagram of volcanic rocks in the study area.

Figure 5 SiO2–K2O diagram of volcanic rocks in the study area.
Figure 5

SiO2–K2O diagram of volcanic rocks in the study area.

Figure 6 A/CNK–A/NK diagram of volcanic rocks in the study area.
Figure 6

A/CNK–A/NK diagram of volcanic rocks in the study area.

The analysis results of major elements in felsic rocks are shown in Table 4. The SiO2 content is between 72.44 and 75.24%, and the aluminum content is moderate, ranging from 12.88 to 14.39%. The content of MgO is 0.27–0.31%, and the content of CaO is 0.26–0.35%. The P2O5 content is low, and the total alkali (ALK) content is high, ranging from 7.66% to 9.13%, with an average of 8.71%. The rocks exhibit sodium-rich characteristics, with the aluminum supersaturation index (A/CNK) ranging from 0.99 to 1.15 and the Rittman index (σ) ranging from 1.81 to 2.81, with an average of 2.46, exhibiting calc-alkaline characteristics. The Mg # value ranges from 17.98 to 22.68, with an average of 20.18. According to the TAS diagram of volcanic rocks (Figure 4), all samples fall within the range of rhyolite. According to the SiO2-K2O diagram (Figure 5), all seven samples are high in potassium/calcium alkaline series rocks. According to the A/CNK-A/NK diagram (Figure 6), it is shown that felsic rocks are mostly weakly peraluminous rocks.

Table 4

Analysis results of major elements (%) and trace elements (ppm) of Rhyolitic tuff in the study area

Sample number H1 H2 H3 H4 H5 H6 H7
Lithology Rhyolitic tuff
SiO2 75.24 73.18 73.10 72.56 72.44 74.82 74.92
TiO2 0.13 0.09 0.12 0.17 0.12 0.15 0.16
Al2O3 13.08 14.39 12.88 14.15 13.64 13.27 13.05
Fe2O3 0.86 0.50 0.64 0.66 0.63 0.56 0.72
FeO 1.11 1.54 1.55 1.64 1.22 1.62 1.28
MnO 0.04 0.03 0.08 0.09 0.10 0.09 0.09
MgO 0.31 0.28 0.27 0.28 0.27 0.29 0.30
CaO 0.35 0.35 0.29 0.30 0.30 0.26 0.30
Na2O 4.32 3.87 4.85 4.66 5.07 4.62 4.61
K2O 3.34 5.11 4.17 4.10 4.07 4.05 4.11
P2O5 0.03 0.03 0.05 0.06 0.05 0.05 0.06
LOI 1.34 0.77 1.32 0.54 0.26 1.73 1.21
TOTAL 100.15 100.14 99.32 99.21 98.17 101.53 100.81
LAK 7.66 8.98 9.02 8.76 9.13 8.67 8.72
Na2O/K2O 1.29 0.76 1.16 1.14 1.25 1.14 1.12
A/CNK 1.15 1.15 0.99 1.12 1.03 1.07 1.04
DI 92.94 92.33 94.5 92.55 94.51 93.64 94.23
σ 1.81 2.67 2.68 2.58 2.81 2.36 2.38
SI 3.12 2.48 2.36 2.43 2.39 2.57 2.72
Mg# 22.68 20.05 18.47 17.98 21.09 19.351 21.62
V 7.42 6.07 6.94 4.35 6.82 4.65 5.92
Cr 2.23 1.98 1.47 1.85 2.05 1.42 1.99
Ni 0.96 0.85 0.88 1.12 0.89 1.00 1.05
Ga 18.71 15.96 18.95 18.91 20.75 17.49 20.47
Rb 91.54 104.67 89.97 95.25 96.01 93.02 86.69
Sr 74.47 158.31 121.38 82.58 80.94 73.36 80.10
Zr 236.82 135.28 182.58 211.66 157.99 148.53 147.82
Nb 11.30 6.66 12.15 14.11 12.51 7.82 9.15
Ba 930.84 1217.76 718.20 1123.00 887.00 999.91 894.06
Hf 7.14 4.07 4.84 5.79 5.40 5.05 5.30
Ta 0.74 0.39 0.95 0.74 0.85 1.04 0.75
W 1.09 0.70 0.44 0.73 0.93 0.89 0.75
Pb 9.03 15.79 12.56 21.31 19.88 13.75 14.49
Th 8.57 4.51 8.78 9.73 9.51 7.80 7.04
U 2.61 1.29 1.88 1.71 1.97 2.83 2.30
La 41.40 15.40 19.31 29.30 21.61 29.46 21.01
Ce 73.70 28.30 45.16 48.01 42.76 62.69 40.81
Pr 9.62 3.46 3.98 3.86 6.27 6.37 6.56
Nd 37.80 13.80 21.67 20.87 26.66 22.99 22.62
Sm 7.65 2.84 3.16 3.39 6.15 3.17 2.92
Eu 1.65 0.62 0.97 0.97 1.51 0.96 0.83
Gd 6.43 2.61 3.04 2.77 4.96 4.74 2.32
Tb 1.13 0.44 0.94 0.87 0.93 0.82 0.78
Dy 7.02 2.85 3.46 5.34 6.16 5.82 5.50
Ho 1.30 0.57 1.12 0.36 0.34 0.80 0.95
Er 3.90 1.70 3.10 1.02 2.03 2.89 3.20
Tm 0.61 0.32 0.34 0.46 0.42 0.30 0.45
Yb 3.90 1.95 2.55 2.38 3.79 2.63 1.94
Lu 0.62 0.32 0.33 0.28 0.47 0.46 0.54
Y 42.50 16.20 36.23 30.73 31.71 19.17 28.54
ΣREE 196.73 75.18 109.13 119.89 124.04 144.10 110.43
LaN/YbN 7.61 5.66 5.42 8.84 4.09 8.03 7.76
δEu 0.72 0.70 0.96 0.97 0.83 0.76 0.98
δCe 0.91 0.95 1.26 1.11 0.90 1.12 0.85

4.2.2 Characteristics of trace and rare earth elements

The analysis results of trace and rare earth elements in trachyandesite are shown in Table 3, and the spider web diagram (Figure 7a) shows the relative enrichment of large ion lithophile elements such as Ba, Rb, and K (LILE) and loss of the high-field-strength elements such as Nb (HFSE). ΣREE = 102.68 × 10−6–171.63 × 10−6, (La/Yb) N = 8.46–12.71, LREE/HREE (the ratio of the sum of La, Ce, Pr, Nd, Sm, and Eu to the sum of Gd, Tb, Dy, Ho, Er, Tm, Yb, and Lu) = 7.68–9.81 (enrichment of light rare earth and depletion of heavy rare earth). Figure 7b shows a clear right-leaning feature. The abnormality of europium is not obvious, with δ Eu = 0.91–1.15 and an average value of 1.02.

Figure 7 Standardized spider diagram of trace elements in the primitive mantle of trachyandesite and standardized distribution pattern diagram of rare earth element of chondrite meteorites.
Figure 7

Standardized spider diagram of trace elements in the primitive mantle of trachyandesite and standardized distribution pattern diagram of rare earth element of chondrite meteorites.

The trace and rare earth element analysis results of rhyolite tuff are shown in Table 4, and the spider of the primitive mantle of the rock web diagram (Figure 7a) shows enrichment of large ion lithophile elements such as Ba, Rb, K, and U and the loss of Nb, Sr, P, and Ti. ∑ REE = 75.18 × 10−6 to 196.73 × 10−6, (La/Yb) N = 4.09–8.84, and some samples have poor heavy rare earth fractionation. Figure 7b shows a clear right-leaning feature. The negative europium anomaly is relatively weak, with a δ Eu value of 0.70–0.98 and an average value of 0.85, which should be the result of plagioclase crystal differentiation. During the formation process of rhyolite tuff, differences in the magma composition, cooling rate, crystallization conditions, and other factors result in variations in the chemical composition, mineral composition, and physical properties of the rock. This difference may manifest in the distribution and dispersion of different data points, as shown in Figure 7b.

5 Discussion

5.1 Zircon chronology

The Late Paleozoic volcanic activity in the Greater Khingan Mountains has always been a focus of research for geologists. In recent years, especially with the continuous advancement of chronological technology, reliable geological chronological data have been provided for the Late Paleozoic volcanic activity and magmatic evolution in the central part of the Xingmeng orogenic belt.

On the Erlian Hegenshan Heihe tectonic belt, a large amount of volcanic and intrusive rocks occurred in the Late Paleozoic era. The measured ages of the intrusive rocks in the Ma Mai Wenduer area of Dongwuqi were 307 ± 1.9 and 299.7 ± 5.3 Ma, and it was believed that they were products of the early extensional structures of the collision between the Siberian plate and the North China plate. The measured age of the intrusive complex was 319.6 ± 4.1 Ma in the Sonazha lead–zinc silver deposit area of Dongwu Banner, which also exhibited an extensional environment [19]. The measured ages of granite in the Dabaoshan area of the Greater Khingan Mountains were 309.0 ± 3.0 and 299.3 ± 2.8 Ma [20]. A study was conducted on the volcanic rocks of the Carboniferous Benbatu Formation in the Chagan Nur area between 313 and 308 Ma and suggested that they may have formed in an extensional environment after the collision, inferring that the Soren suture zone had closed before the Late Carboniferous [21].

In this study, zircon U–Pb dating was carried out on moderately felsic volcanic rocks, avoiding the metamorphic clastic rocks in the lower part. Zircon particles with good crystallization and obvious magmatic zircon characteristics were selected. The zircon U–Pb age of intermediate trachyandesite was 304.4 ± 2.3 Ma, and that of rhyolite tuff was 307.6 ± 2.0 Ma, representing the age of volcanic rock formation. There is a certain time interval between the two. Based on a comprehensive analysis of the profile, it is believed that the region experienced a relatively complete sedimentary eruption cycle in the Late Carboniferous. First, a marine sedimentary layer dominated by terrestrial debris was formed in low-lying areas in the early stages, followed by the strongest period of volcanic activity. Alkaline magma erupted effusively on a large scale, accompanied by jet eruptions of medium felsic magma, forming a rock combination mainly composed of trachyandesite and trachyte interbedded with andesitic tuff. Then, felsic magma erupted on a large scale, mainly consisting of rhyolite tuff. Based on zircon U–Pb chronology, this volcanic rock group was determined to be the Late Carboniferous Gegenaobao Formation.

5.2 Source characteristics

The volcanic rocks in the northwest region of Zhalaite Banner are mainly composed of intermediate trachyandesite, felsic rhyolite, and tuff. Compared to felsic rocks, intermediate trachyandesite has higher MgO, CaO, and P2O5 content, while felsic rocks have higher total alkali (ALK) content and higher K2O/Na2O values with similar aluminum content. The content of intermediate rocks is similar to that of trachyandesite measured, while the content of felsic rocks is similar to that of rhyolite in Tonglu, Zhejiang, and Xiangshan, Jiangxi [22]. According to the measured content of major elements in the volcanic rocks, the values of the high potassium/calcium alkaline series rocks in the island arc volcanic rocks are similar [23], suggesting that the volcanic rocks are related to a volcanic arc magmatic activity.

According to the spider diagram of trace elements and the rare earth element distribution diagram (Figure 7), the volcanic rocks are relatively enriched in light rare earth elements and large ion lithophilic elements such as Ba, K, and Rb, significantly losing high field strength elements such as Nb, especially felsic rocks that strongly lose Sr, P, and Ti. In island arc or active continental margin environments, volcanic rocks are enriched in light rare earth elements and large ion lithophile elements, while they are depleted in high field strength elements, are often formed due to magmatic activity caused by plate subduction, suggesting that magma may have originated from crustal melting [24,25]. The volcanic rocks and intermediate rocks in the research area have subtle Eu anomalies, δEu = 0.91–1.15, the average value is 1.02, and the Sr anomaly is not obvious, while the felsic rock shows a more obvious Eu anomaly with an average value of 0.63. At the same time, the Sr anomaly is also significantly deficient compared to the intermediate rock, which is consistent with the observation data under the petrological microscope in a previous report. The plagioclase content of the intermediate rock is significantly lower than that of the felsic rock. The negative anomaly of P may manifest as the crystallization separation of apatite, while the depletion of Ti may be controlled by the separation crystallization of ilmenite. The negative anomalies of Sr and Ba indicate that plagioclase may have undergone fractional crystallization. Similarly, the separation and crystallization of plagioclase can lead to a strong depletion of Eu and Sr, which are strongly compatible elements with plagioclase. The negative anomaly of P indicates the separation and crystallization of apatite during magma evolution, while the negative anomaly of Nb suggests the possible involvement of crustal material in magma evolution. The intersecting phenomenon of the trace-element bead network curves is due to the varying degrees of enrichment of individual elements in different rocks, reflecting the addition or contamination of external substances during magma migration and diagenesis. These are typical characteristics of crustal magma being contaminated by upper crustal materials [26].

The average Nb/U value of intermediate volcanic rocks is 9.16, while that of felsic rocks is 5.33, which is lower than the continental crust [25]. The average Nb/Ta ratio is 16.45 (except for a lower sample), which is significantly higher than the average value of the continental crust [27] and closer to the corresponding value of 17.8 in the original mantle, suggesting the presence of mantle-derived magma involvement. The average Ba/Th values of trachyandesite are 250.10, Ba/La values are 35.27, La/Nb values are 3.08, and Ba/Nb values are 109.15, which are all higher than those of oceanic ridge basalt (N-MORB) originating from the depleted mantle, with values of 60, 4, 1.07, and 4.3, respectively, and generally higher than the average level of continental crust. It is generally believed that the La/Nb ratio is high, which is also a distinct feature of contamination [28,29]. The average Rb/Sr ratio of felsic rocks is 1.05 (greater than 0.5), the average Ti/Zr ratio is 4.72 (less than 20), and the average Ti/Y ratio is 29.65 (mostly less than 100), all of which belong to the characteristics of crustal magma products.

Compared with basalt magma, andesite magma has a more complex source and can be formed through partial melting of the metasomatic mantle. This type of magma has not undergone significant evolution, so its rare earth element chondrite standardization map shows a U-shaped curve. It can also be directly melted through the subduction of the oceanic crust [30]. In this case, the rare earth element distribution map of volcanic rocks will have a steep right-leaning feature, with strong light and heavy rare earth fractionation, especially the loss of heavy rare earth elements [31]. If the solution produced by oceanic crust melting interacts with mantle rocks during the ascent process, it will form high magnesium andesite, and the content of heavy rare earth elements will significantly increase. Basalt, andesite, and even felsic rocks produced under the background of island arcs are mostly caused by the crystallization differentiation of basic magma. Under the background of land arcs, the thickness of the crust is large, which provides a longer crystallization differentiation time for a large amount of basic magma to rise. The rocks produced under these conditions have obvious negative europium anomalies, mainly due to the crystallization differentiation of plagioclase. The traditional belief is that rhyolite rocks are products of crustal material melting. In recent years, research has found that felsic island arc magmas can also be formed by the melting process of subducting oceanic crust [32]. The Y value content of felsic rocks in this study is relatively high, averaging 29.30, and the degree of differentiation between light and heavy rare earths is low, averaging 6.49. Therefore, the volcanic rocks in the study area are more likely to come from partial melting of the crust. At the same time, according to the C/MF–A/MF diagram of volcanic rocks (Figure 8), most of the intermediate trachyandesite comes from the partial melting of basic rocks with deeper sources. Felsic rocks originate from the partial melting of metamorphic mudstone.

Figure 8 Harker diagram of volcanic rocks in the study area.
Figure 8

Harker diagram of volcanic rocks in the study area.

In order to distinguish the source of magma, the Mg# value is an ideal parameter. Studies have shown that the typical midocean ridge tholeiitic basalt (MORB) has an Mg# value of about 60. However, according to experimental petrological research, the Mg# value of lower crust-derived solutions is relatively low and has little correlation with the degree of melting, generally less than 40. Only with the participation of mantle material can the Mg# value be greater than 40. The Mg# values of the intermediate trachyandesite studied in this study are 30.23–49.53, with an average of 41.98, indicating that it is mainly a product of crustal magma with slight involvement of mantle material. Mg# values of felsic rocks are 17.98–22.68, with an average of 20.18, indicating typical characteristics of crustal magma.

Based on comprehensive analysis, it is believed that the volcanic rocks in the study area mainly originate from the crust, but the composition of intermediate rocks should be partially melted by mantle material. The formation age of intermediate rocks is 304.4 ± 2.3 Ma, and the formation age of felsic rocks is 307.6 ± 2.0 Ma. The two are relatively close. At the same time, according to the actual occurrence of the field strata, both have continuity in time and space, and the two should be a relatively continuous eruption sedimentary environment.

5.3 Construction environment

The Xingmeng orogenic belt in central Inner Mongolia is characterized by strong Paleozoic accretion and strong Mesozoic Cenozoic transformation and is an important component of the eastern section of the Central Asian orogenic belt in China. The formation and development of the Xingmeng orogenic belt are closely related to the evolution of the ancient Asian Ocean. This study area is located in the northwest of Zhalaite Banner in eastern Inner Mongolia, slightly west of the contact zone between the Xing’an block and the Songnen block, and is an ideal place for studying the magmatic activity of the Xingmeng orogenic belt.

The ancient Asian Ocean did not simply continue to subduct until the end of the collision but went through long and multiple stages of subduction extension before finally colliding and closing, completing the transition toward the continental crust [33]. The Songnen block merged with the Duobaoshan Island Arc along the Heihe Zhalantun line during the Late Carboniferous, gradually forming a land area with the Xing’an Songnen block in the middle. The structural pattern of the Okhotsk Ocean to the north and the Paleo-Asian Ocean to the south continued until the Middle Permian. Early Carboniferous metamorphic basic volcanic rocks were discovered in the Xilinhot area, suggesting that the controlled primitive magma formation of this volcanic rock originated from the depleted mantle of the subduction plate dehydration metasomatism and was a product of magmatic activity in the island arc environment. They inferred that the ancient Asian Ocean was not closed during the Early Carboniferous but was still in the stage of subduction and subduction of the oceanic crust [34].

The volcanic rocks in this study area were formed during the Late Carboniferous, and according to zircon U–Pb dating data, they were formed between 304 and 308 Ma. Similarly, there have been numerous reports of volcanic magmatism during the Late Carboniferous in areas such as Xilinhot, Suzuoqi, and Dongwuqi in the Greater Khingan Mountains [35], suggesting that the occurrence of volcanic magmatism during the Late Carboniferous had a certain degree of isochronicity.

According to data, there are a total of six ancient subduction zones in Inner Mongolia, among which the Hegenshan Zhalantun accretion complex belt is located in the southern part of the study area, extending northeast. This is also an extension of the Erlian Hegenshan Heihe ophiolite complex belt, with an overall trend of NE, which is consistent with the direction of the main structural line in the area. There are a large number of A-type granites distributed around this tectonic zone; therefore, there is also a certain spatial connection between the Late Carboniferous magmatic rocks.

According to the latest chronological and geochemical data, A-type granite in the Xing’an Island Arc was formed during the Late Carboniferous. The measured age of alkaline granite in the Ulan Tolgoi area was 317 Ma [36], and the age of alkali feldspar granite in the Duobao Mountain area was 309 Ma. The measured age of potassium feldspar granite in the Twelve Stations rock mass in the Heihe area of the northeastern part of the Daxing’an Mountains was 298 Ma. The measured age of granite in the Jinggetai area of Inner Mongolia was 301 Ma [37]. At the same time, there is also a distribution of I-type granite with high differentiation on a certain scale in the Zhalantun area, such as the 322 Ma syenogranite in Quansheng Forest Farm and the 317–314 Ma syenogranite in the Tayuan area [38], indicating that the intrusive rocks formed during this period have a post-orogenic extensional background. The felsic volcanic rocks in this study also exhibit high differentiation characteristics, suggesting that they may also have extensional backgrounds. They found in their study of the Nenjiang area on the southeastern edge of the Xing’an block that the age of the intermediate felsic intrusive rocks in the area was between 315 and 298 Ma, formed during the Late Carboniferous. They also compared the magmatic activity of the Early Carboniferous and concluded that the Xingmeng orogenic belt experienced two distinct periods of magmatic activity during the Carboniferous, belonging to different tectonic backgrounds. The Early Carboniferous was in a subduction environment, while the Late Carboniferous was in an extensional tectonic environment after plate collision [39]. It is believed that the differentiated I- and A-type granites distributed in the Zhalantun area are a sign of vertical crustal thickening in the region, with strong post-collisional magmatic activity [40].

At the end of the Early Carboniferous, the Siberian Plate and the North China Plate contracted and eventually collided, forming a large amount of Early Carboniferous magmatic rocks in the Hegenshan Heihe tectonic zone. Subsequently, the ancient Asian oceanic crust in the middle of the Late Carboniferous subducted and subducted northwestward along the Hegenshan Zhalantun line, causing the collision and merging of the Xing’an Block and the Songnen Block on the southern edge of the Siberian Plate. To the north of the subduction zone, a volcanic rock combination related to subduction gradually formed in the Yiershi Diannan area, reflecting the continental margin volcanic arc environment. Subsequently, in the late Carboniferous to early Permian of the Xing’an Island Arc, magmatic rocks with highly differentiated Type I and Type A and post-orogenic collision extensional environments gradually formed.

The lg σ–Lg τ diagram shows that the volcanic rocks in the study area are mainly located within the range of the subduction zone (Figure 9a). According to the Hf Ta Th and Yb + Ta Rb diagrams, the volcanic rocks belong to the range of island arc rocks, especially felsic volcanic rocks with post-collision characteristics (Figure 9b and c). The Ta/Yb and Th/Yb diagrams show an active continental margin arc, indicating that subduction is still ongoing (Figure 9d). Based on comprehensive analysis, it is believed that the volcanic rocks in the study area should be related to volcanic magmatic events with continental arc characteristics during the subduction process of the oceanic crust. At the same time, volcanic rocks have crustal characteristics, while intermediate rocks have deeper magma sources and the participation of mantle-derived materials. Felsic rocks have high heterogeneity, indicating a post-collision extensional environment background. This indicates that in the late Carboniferous, the Songnen block and Xing’an block have completed integration, and the Xingmeng orogenic belt gradually transitioned toward a post-collision extensional environment.

Figure 9 Structure diagram of volcanic rocks in the study area: (a) lg σ–lg τ; (b) Hf–Ta–Th; (c) Yb+Ta–Rb; and (d) Ta/Yb–Th/Yb.
Figure 9

Structure diagram of volcanic rocks in the study area: (a) lg σ–lg τ; (b) Hf–Ta–Th; (c) Yb+Ta–Rb; and (d) Ta/Yb–Th/Yb.

In summary, the study area underwent three stages of development during the Late Paleozoic era. The first stage is the closure stage of the ancient Asian Ocean from the Late Devonian to the Carboniferous, characterized by a tectonic environment based on oceanic crust and an active continental margin environment with magma development (Figure 10a). The second stage is the land–land collision stage of the Late Carboniferous, during which the study area received intermediate and felsic volcanic rock deposits with island arc properties from the Gegen Aobao Formation. Analysis suggests that this should be a product of further activation of land–land collision by the movement of the two major plates in the north and south (Figure 10b). In the folding and orogeny stage of the Early Middle Permian in the third stage, the crust underwent folding and orogeny, causing the volcanic rock layers of the Gegen Aobao Formation to fold and then the crust to rise, resulting in sedimentary interruptions in the Early Middle Permian (Figure 10c).

Figure 10 Late Paleozoic regional tectonic evolution model. (a) The closure stage of the ancient Asian Ocean from the Late Devonian to the Carboniferous; (b) the stage of land–land collision in the Late Carboniferous; and (c) the fold orogeny stage of the Early Middle Permian.
Figure 10

Late Paleozoic regional tectonic evolution model. (a) The closure stage of the ancient Asian Ocean from the Late Devonian to the Carboniferous; (b) the stage of land–land collision in the Late Carboniferous; and (c) the fold orogeny stage of the Early Middle Permian.

6 Conclusions

  1. The zircon LA-ICP-MS U–Pb ages of the intermediate felsic volcanic rock combination in the Zhalaiteqi area of eastern Inner Mongolia are 304.4 ± 2.3 Ma and 307.6 ± 2.0 Ma, respectively. The formation period is the Late Carboniferous.

  2. The Late Carboniferous volcanic rocks in this study area are relatively enriched in light rare earth elements and large ion lithophile elements such as Ba, K, and Rb while significantly losing high field strength elements such as Nb. Particularly, felsic rocks strongly lose Sr, P, and Ti. It is believed that the magma of this volcanic rock combination mainly originates from the crust, but the composition of intermediate rocks should be partially melted by mantle material, and felsic rocks may have been contaminated by shallow crustal material. Both are tectonic environments of continental margin arc volcanic rocks, exhibiting magmatic activity events related to subduction extension.

  3. The felsic volcanic rocks of the Gegenaobao Formation in the northwest of Zhalaite Banner are located on the Late Paleozoic A-type magmatic rock belt along the Erlian Hegenshan Zhalantun Heihe line. Based on rock assemblages, chronology, and geochemical characteristics, comprehensive analysis suggests that the Xing’an block and Songnen block have completed collision and assembly in the Early Carboniferous and were in a tectonic environment of subducted continental arc volcanoes in the Late Carboniferous with post-orogenic extension characteristics. The Late Carboniferous ancient Asian Ocean has closed along the Erlian Hegenshan Zhalantun Heihe rock structural belt in the north, and the Xingmeng orogenic belt has begun to enter the stage of orogenic extension.

Acknowledgments

This work was funded by the basic Geological Survey Project of Shenyang Geological Survey Center “Inner Mongolia 1:50000 Diaoyutai (L51E006006), Chuludaba (L51E006007), Dongbayan Ulan (L51E006008), Taladaba (L51E005008) regional geological survey.” The authors thank Dr. Wei Zhou and Dr. Kunyu Wu from the School of Earth and Environmental Sciences of the University of Queensland for help in the revision of the main part of this manuscript. The authors also thank the editor and reviewers for their assistance with this manuscript.

  1. Funding information: This work was supported by 2024 Guangxi University Young and Middle aged Teachers Basic Scientific Research Ability Improvement Project (2024KY0813); and the Doctor and Professor Foundation of Guilin University of Aerospace Technology (KX202204801).

  2. Author contributions: Drawing of graphics: Wang Li, Wang Guanhong. Data processing: Tang Xinglong, Li Zhuang. Writing – original draft: Liang Tianyi. Writing – review & editing: Li Mengmeng.

  3. Conflict of interest: Authors state no conflict of interest.

  4. Data availability statement: Data sharing is not applicable to this article as no datasets were generated or analysed during the current study.

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Received: 2024-09-10
Revised: 2025-02-11
Accepted: 2025-02-28
Published Online: 2025-04-07

© 2025 the author(s), published by De Gruyter

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

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https://doi.org/10.1515/geo-2025-0786
Schlagwörter für diesen Artikel
U-Pb chronology; rock geochemistry; Xingmeng orogenic belt; magmatic genesis
Creative Commons
BY 4.0

Artikel in diesem Heft

  1. Ionization hotspots near waterfalls in Eastern Serbia’s Stara Planina Mountain
  2. Research Articles
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  94. YOLO-MC: An algorithm for early forest fire recognition based on drone image
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  100. Streamlining digital elevation model construction from historical aerial photographs: The impact of reference elevation data on spatial accuracy
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  110. Ore-controlling structures of granite-related uranium deposits in South China: A review
  111. Shallow geological structure features in Balikpapan Bay East Kalimantan Province – Indonesia
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  113. Special Issue: Natural Resources and Environmental Risks: Towards a Sustainable Future - Part II
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  115. Special Issue: Geospatial and Environmental Dynamics - Part II
  116. Advancing urban sustainability: Applying GIS technologies to assess SDG indicators – a case study of Podgorica (Montenegro)
  117. Spatiotemporal and trend analysis of common cancers in men in Central Serbia (1999–2021)
  118. Minerals for the green agenda, implications, stalemates, and alternatives
  119. Spatiotemporal water quality analysis of Vrana Lake, Croatia
  120. Functional transformation of settlements in coal exploitation zones: A case study of the municipality of Stanari in Republic of Srpska (Bosnia and Herzegovina)
  121. Hypertension in AP Vojvodina (Northern Serbia): A spatio-temporal analysis of patients at the Institute for Cardiovascular Diseases of Vojvodina
  122. Regional patterns in cause-specific mortality in Montenegro, 1991–2019
  123. Spatio-temporal analysis of flood events using GIS and remote sensing-based approach in the Ukrina River Basin, Bosnia and Herzegovina
  124. Flash flood susceptibility mapping using LiDAR-Derived DEM and machine learning algorithms: Ljuboviđa case study, Serbia
  125. Geocultural heritage as a basis for geotourism development: Banjska Monastery, Zvečan (Serbia)
  126. Assessment of groundwater potential zones using GIS and AHP techniques – A case study of the zone of influence of Kolubara Mining Basin
  127. Impact of the agri-geographical transformation of rural settlements on the geospatial dynamics of soil erosion intensity in municipalities of Central Serbia
  128. Where faith meets geomorphology: The cultural and religious significance of geodiversity explored through geospatial technologies
  129. Applications of local climate zone classification in European cities: A review of in situ and mobile monitoring methods in urban climate studies
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Heruntergeladen am 7.10.2025 von https://www.degruyterbrill.com/document/doi/10.1515/geo-2025-0786/html?srsltid=AfmBOoqYlRIXZJ9_EH9RDXaTHEgq0MrBRcRUVvqmbVH6MF0SudDuXvXp
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