Home Late Jurassic Haobugao granites from the southern Great Xing’an Range, NE China: Implications for postcollision extension of the Mongol–Okhotsk Ocean
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Late Jurassic Haobugao granites from the southern Great Xing’an Range, NE China: Implications for postcollision extension of the Mongol–Okhotsk Ocean

  • Jianda Li EMAIL logo , Yue Tian and Yuqi Cheng
Published/Copyright: November 13, 2023
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Open Geosciences
From the journal Open Geosciences Volume 15 Issue 1

Abstract

The Mongolia-Okhotsk tectonic regime had a significant impact on the tectonic evolution of Northeastern (NE) China. However, there is no consensus on the role of this regime in the geological evolution of the Xing’an Massif during the late Mesozoic. This article presents the results of zircon U–Pb geochronology, whole-rock major and trace-element geochemistry, and zircon Hf isotopic compositions for granites in the Haobugao area of the southern Great Xing’an Range, NE China, to determine their petrogenesis, source, and tectonic setting. The zircon U–Pb ages indicate that the granites crystallized at 152.7 ± 0.5 Ma. The granites exhibit high SiO2 (70.75–73.19 wt%) and K2O + Na2O (8.00–8.65 wt%) contents and extremely low MgO (0.40–0.59 wt%) and TiO2 (0.24–0.33 wt%) contents. They belong to the metaluminous, high-K calc-alkaline, and ferroan series, with mostly right-inclined REE curves, flat heavy rare earth element patterns, high 10,000 Ga/Al ratios, and intensely negative Eu anomalies. The Zr/Hf ratios are 24.2–27.7, Nb/Ta ratios are 6.4–8.9, and Y/NbN ratios are >1.2. These characteristics suggest an A2-type granite affinity. The zircon εHf values of the rocks range from +5.62 to +9.12, corresponding to T DM2 values of 621–906 Ma, indicating that juvenile materials in the Neoproterozoic may be a source of these granites. Geochemically, these Late Jurassic A2-type granites are similar to those from post-collision extension settings. The primary magma was likely derived from the partial melting of a delaminated region of the lower crust.

Keywords: Xing’an Massif; Late Jurassic; A2-type granites; petrogenesis; geochronology; geochemistry; Mongol–Okhotsk oceanic plate

1 Introduction

Northeast (NE) China is generally considered to be the eastern part of the Central Asian Orogenic Belt (CAOB). The rocks in NE China constitute one of the most remarkable geological features of the eastern margin of the Asian continent and have become a hot research topic in recent years, due to their significance in deciphering the tectonic evolution of the CAOB [1−7]. The southern Great Xing’an Range (SGXR) is located in the eastern part of the CAOB, which was affected by the closure of the Mongolia-Okhotsk Ocean and paleo-Pacific subduction from the Late Jurassic to the Cretaceous period [6−11]. Previous studies have suggested that extensive late Mesozoic magmatism in NE China was related to the subduction of the Paleo-Pacific oceanic plate, and the Mongol–Okhotsk oceanic plate had subducted northwards beneath the southern margin of the Siberian Craton during late Mesozoic [12,13]. However, several recent studies of Mesozoic calc-alkaline volcanic belts along the southern margin of the Mongol–Okhotsk Suture Belt in the SGXR indicate intrusions of Mongol–Okhotsk oceanic plate and southward subduction beneath the Erguna Massif during this period, highlighting the role of the Mongol–Okhotsk Ocean [8,14,15]. Thus, this extensive late Mesozoic magmatism may be influenced by the Paleo-Pacific oceanic plate or the closure of the Mongol–Okhotsk Ocean and there is no consensus on the geodynamic setting of late Mesozoic magmatism in NE China [8,9,16,17,18].

The influence of the Mongol–Okhotsk tectonic regime on the Greater Xing’an Range has not been extensively studied, and the tectonic setting of Mesozoic volcanic rocks and their spatiotemporal relationships with varied orogenic systems in NE China is unclear. In this article, we present new zircon LA-ICP-MS U–Pb ages for the granites in the Haobugao area of the SGXR in NE China. We used whole-rock major and trace-element geochemistry, zircon Hf isotopic data, and petrological observations to constrain the petrogenesis of the granites. These data provide new insights into the sources and offer significant contributions to the understanding of the Jurassic tectonic evolution of the Great Xing’an Range.

2 Geological background and sample descriptions

NE China is primarily composed of a Paleozoic orogenic collage that forms part of the eastern segment of the CAOB [19], as shown in Figure 1a. This region has undergone the evolution of the Paleo-Asian, Mongol–Okhotsk, and Paleo-Pacific oceans [6,9,19,20,21], along with the amalgamation of several micro-continental blocks or terranes during the Phanerozoic, including the Erguna, Xing’an, Songliao, and Jiamusi-Khanka blocks [9,16] (Figure 1b).

Figure 1 (a) Schematic map of the CAOB (modified after Ouyang et al. [27]), showing the location of NE China; (b) tectonic sketch map of NE China, modified after Wu et al. [33]. (c) Sketch geological map of magmatic rock distribution, modified after Wang et al. [8]. (1) Late Yanshanian granitoids; (2) Early stage of Late Yanshanian granitoids; (3) Early Yanshanian granitoids; (4) Indosinian granitoids; (5) Late Hercynian granitoids; (6) Middle Hercynian granitoids; (7) Ultrabasic rock; (8) Fault; (9) Copper deposit; (10) Lead zinc deposit; (11) Copper molybdenum deposit; (12) Tin iron deposit; (13) Tungsten tin deposit; (14) Rare earth element deposit; (15) Tin copper deposit; (16) Silver deposit; and (17) Gold deposit.
Figure 1

(a) Schematic map of the CAOB (modified after Ouyang et al. [27]), showing the location of NE China; (b) tectonic sketch map of NE China, modified after Wu et al. [33]. (c) Sketch geological map of magmatic rock distribution, modified after Wang et al. [8]. (1) Late Yanshanian granitoids; (2) Early stage of Late Yanshanian granitoids; (3) Early Yanshanian granitoids; (4) Indosinian granitoids; (5) Late Hercynian granitoids; (6) Middle Hercynian granitoids; (7) Ultrabasic rock; (8) Fault; (9) Copper deposit; (10) Lead zinc deposit; (11) Copper molybdenum deposit; (12) Tin iron deposit; (13) Tungsten tin deposit; (14) Rare earth element deposit; (15) Tin copper deposit; (16) Silver deposit; and (17) Gold deposit.

During the Paleozoic and possibly extending into the Early-Middle Triassic, the tectonic development of NE China was controlled by the Paleo-Asian Ocean, which was characterized by crustal accretion and micro-block and terrane amalgamations [19,22,23]. Recent studies suggested that the final closure of the Paleo-Asian Ocean, marked by suturing between the Songliao block and the Liaoyuan terrane, may have occurred at around 230 Ma [21]. In the Mesozoic, NE China experienced the superposition of the Mongol–Okhotsk Ocean and Paleo-Pacific tectonic regimes [8,9,10,16,24]. During this period, abundant granitic rocks were exposed in NE China, covering an area of approximately 200,000 km2 [9]. Geochemical data from these granitic rocks indicate that they contain a high proportion of mantle-derived materials and record significant Phanerozoic crustal growth, as shown by their low initial Sr and positive initial Nd and Hf isotopic values, and young model ages, regardless of their spatial and temporal distribution [25,26]. However, it is still unclear whether crustal growth took place during orogenic, post-orogenic, or even anorogenic stages during the evolution of NE China and the Great Xing’an Range [27].

The Haobugao area is situated in the SGXR (Figure 1c) which is bordered by the Erlian-Hegenshan fault to the north, the Xar Moron fault to the south, and the Nenjiang fault to the NE. The Mesozoic granitoids in the Great Xing’an Range consist of granodiorite, monzogranite, alkali granite, and syenogranite, with ages ranging from 255–220 Ma (Early–Middle Triassic), 184–160 Ma (Early–Middle Jurassic), and 155–120 Ma (Late Jurassic–Early Cretaceous) (Figure 2). The Early–Middle Triassic granitoids were most likely related to post-orogenic lithospheric extension after the closure of the Paleo-Asian Ocean [28], while there is still no consensus regarding the geodynamic setting for the younger two granitoid groups [6,9,16,29]. The debate has mainly focused on questions concerning the spatial and temporal extent to which the Mongol–Okhotsk and Paleo-Pacific tectonic regimes influenced events in the SGXR, as this region was affected by both these tectonic regimes during the late Mesozoic. The volcanic rocks in the SGXM are mainly distributed in several discrete basins, including the Baoshi, Pingshan, and Wudan basins, and have been subdivided into the Manketouebo, Manitu, Baiyingaolao, Dashizai, and Meiletu formations [30]. Field observations suggest that the Haobugao granite outcrops are in intrusive contact with intermediate–acidic volcanic rocks of the lower Permian Dashizhai Formation and are unconformably overlain by acidic volcanic rocks of the Lower Cretaceous Manketouebo Formation (Figure 2).

Figure 2 Detailed geological map of the Haobugao area, showing sample location.
Figure 2

Detailed geological map of the Haobugao area, showing sample location.

The major minerals of Haobugao granites are K-feldspar (25–30%), quartz (Q) (25–30%), plagioclase (35–40%), and biotite (Bt) (≤3%, interstitial) along with accessory zircon, apatite, and magnetite (Figure 3). All the samples exhibit a medium- to fine-grained (0.5–3 mm) granitic texture and massive structure.

Figure 3 Photomicrographs and hand specimen show representative lithologies of the Haobugao granites. (a) Thin section photograph of monzogranite (sample H-08, cross-polarized light); (b) thin section photograph of monzogranite (sample H-8, cross-polarized light); and (c) hand specimen (sample H-8). Abbreviations: Q, quartz; PI, plagioclase; Kfs = potassium feldspar; Bt = biotite.
Figure 3

Photomicrographs and hand specimen show representative lithologies of the Haobugao granites. (a) Thin section photograph of monzogranite (sample H-08, cross-polarized light); (b) thin section photograph of monzogranite (sample H-8, cross-polarized light); and (c) hand specimen (sample H-8). Abbreviations: Q, quartz; PI, plagioclase; Kfs = potassium feldspar; Bt = biotite.

3 Analytical methods

3.1 Zircon U–Pb dating

Zircons were selected from whole-rock samples by magnetic separation and heavy-liquid separation methods using a binocular microscope in the Langfang Regional Geological Survey of Hebei Province, China. The samples were then pasted on epoxy resin and analyzed by zircon cathodoluminescence (CL) imaging. According to the CL images of zircon, U–Pb dating was carried out by secondary ion mass spectrometry (SIMS). SIMS zircon U–Pb analyses were conducted on the CAMECA IMS-1280 ion microprobe at Beijing Yanduzhongshi Geological Analysis Laboratory. The absolute abundances of U–Th–Pb isotopes and their ratios were determined relative to the standard zircon 91500 [31], using the operating and data processing procedures similar to those described by Xie et al. [32].

3.2 Major and trace-element analyses

For geochemical analyses, whole-rock samples were reduced to 200 mesh after removing the weathering surfaces. The major and trace elements of the whole rock were tested at Yanduzhongshi Geological Analysis Laboratories, Beijing, by X-ray fluorescence spectrometry and inductively coupled plasma-mass spectrometry (ICP-MS), after acid digestion of the samples in Teflon bombs.

3.3 Zircon Hf isotopic compositions

Zircon in situ Lu–Hf isotope dating was conducted using a Neptune multicollector-ICP-MS (MC-ICP-MS) with an ArF excimer laser ablation system at Beijing Yanduzhongshi Geological Analysis Laboratory. The test procedure and calibration method were similar to those used by Wu et al. [33]. Lu–Hf analyses were performed on the same zircon grains as analyzed for U–Pb, with ablation pits, 30 μm in diameter, a laser energy density of 16 J cm−2, an ablation time of 31 s, and repetition rates of 8 Hz. The detailed operating conditions for the laser ablation system and the MC-ICP-MS instrument and analytical method are the same as those described by Hu et al. [34].

4 Results

4.1 Zircon U–Pb ages

The zircons from the granites are euhedral–sub-euhedral structures, with particle sizes ranging from 85 to 185 μm, and show relatively clear oscillatory growth zoning in CL images (Figure 4), indicating that they are products of magmatic crystallization. Twenty-four zircons were selected for the U–Pb test. Th (345 × 10−6–2,724 × 10−6) and U (165 × 10−6–1,235 × 10−6) in the zircon grains vary greatly. Th/U ranged from 0.28 to 0.48, which is consistent with typical magmatic zircon. The 206Pb/238U age was between 149 and 157 Ma (Table 1). On the Concordia diagram and weighted average diagram (Figure 5), the distribution of the 24 zircon points was concentrated, and the mean age was 152.7 ± 0.52 Ma (mswd = 0.1), which is interpreted as the formation age of the granites.

Figure 4 Representative CL images of zircons from the Haobugao granites. Red and white circles indicate the locations of LA-ICP-MS U–Pb analyses and Lu–Hf isotopic analyses, respectively.
Figure 4

Representative CL images of zircons from the Haobugao granites. Red and white circles indicate the locations of LA-ICP-MS U–Pb analyses and Lu–Hf isotopic analyses, respectively.

Table 1

LA-ICP-MS zircon U–Pb dating data for the Haobugao granites

No. U Th Pb Th/U 207Pb/206Pb 207Pb/235U 206Pb/238U 207Pb/206Pb 207Pb/235U 206Pb/238U
ppm Ratio 1σ Ratio 1σ Ratio 1σ Age (Ma) 1σ Age (Ma) 1σ Age (Ma) 1σ
1 2012.78 665.39 175.15 0.33 0.04915 0.00060 0.16343 0.00305 0.02413 0.00039 155 28 154 3 154 2
2 2648.21 844.94 230.38 0.32 0.04853 0.00060 0.16184 0.00323 0.02408 0.00035 125 29 152 3 153 2
3 1427.06 680.59 114.68 0.48 0.04963 0.00078 0.16632 0.00445 0.02410 0.00042 178 37 156 4 154 3
4 1680.00 538.53 152.39 0.32 0.05080 0.00106 0.16824 0.00437 0.02401 0.00056 232 48 158 4 153 4
5 429.98 210.76 37.70 0.49 0.05047 0.00178 0.16345 0.00534 0.02359 0.00035 217 82 154 5 150 2
6 2589.07 874.78 222.67 0.34 0.04869 0.00057 0.16175 0.00312 0.02402 0.00038 133 28 152 3 153 2
7 1871.84 575.40 157.73 0.31 0.04949 0.00069 0.16343 0.00308 0.02382 0.00030 171 33 154 3 152 2
8 1857.19 522.71 156.73 0.28 0.04758 0.00069 0.16275 0.00412 0.02471 0.00048 78 34 153 4 157 3
9 1258.20 417.52 107.43 0.33 0.04907 0.00064 0.16354 0.00302 0.02413 0.00036 151 31 154 3 154 2
10 1621.25 484.58 137.38 0.30 0.04894 0.00084 0.16024 0.00296 0.02371 0.00029 145 40 151 3 151 2
11 3229.34 977.62 273.79 0.30 0.04941 0.00064 0.16363 0.00346 0.02404 0.00049 167 30 154 3 153 3
12 2210.69 623.90 190.75 0.28 0.04798 0.00070 0.16024 0.00354 0.02413 0.00040 98 35 151 3 154 3
13 2976.09 953.26 246.92 0.32 0.05039 0.00128 0.16226 0.00432 0.02334 0.00045 213 59 153 4 149 3
14 1607.95 503.53 141.93 0.31 0.04927 0.00111 0.16440 0.00447 0.02417 0.00032 161 53 155 4 154 2
15 2369.81 762.83 207.92 0.32 0.04837 0.00067 0.16007 0.00270 0.02409 0.00040 117 33 151 2 153 3
16 1431.48 523.59 121.29 0.37 0.04883 0.00075 0.16097 0.00411 0.02377 0.00037 140 36 152 4 151 2
17 4078.89 1253.07 344.01 0.31 0.04928 0.00064 0.16250 0.00336 0.02390 0.00045 161 30 153 3 152 3
18 1904.22 554.41 164.72 0.29 0.04842 0.00068 0.16172 0.00302 0.02426 0.00042 120 33 152 3 155 3
19 1634.54 624.65 140.24 0.38 0.04867 0.00069 0.16169 0.00299 0.02421 0.00042 132 34 152 3 154 3
20 715.67 242.42 57.14 0.34 0.04888 0.00122 0.16152 0.00528 0.02377 0.00036 142 59 152 5 151 2
21 1790.37 543.34 152.96 0.30 0.04816 0.00080 0.15973 0.00443 0.02407 0.00057 107 39 150 4 153 4
22 3086.01 910.41 227.76 0.30 0.04969 0.00077 0.16327 0.00367 0.02389 0.00051 181 36 154 3 152 3
23 2049.18 490.37 152.69 0.24 0.04989 0.00162 0.16558 0.00488 0.02397 0.00044 190 76 156 4 153 3
24 2097.65 656.80 181.66 0.31 0.04991 0.00079 0.16480 0.00383 0.02390 0.00043 191 37 155 3 152 3
Figure 5 Zircon U–Pb concordia diagram (a) and weighted average diagram (b) for the Haobugao granites.
Figure 5

Zircon U–Pb concordia diagram (a) and weighted average diagram (b) for the Haobugao granites.

4.2 Whole-rock major- and trace-element geochemistry

Table 2 lists the results of whole-rock major and trace elements. The Haobugao granites have high SiO2 (70.75–73.19%), K2O (4.31–5.03%), Na2O (4.21–4.66%) contents, and Na2O + K2O values (8.00–8.65%). The Al2O3, TiO2, and P2O5 contents were 13.42–14.13%, 0.24–0.33%, and 0.07–0.10%, respectively. In the total alkali versus SiO2 diagram (Figure 6a), all samples fell in the range of granite. The A/CNK varied from 0.88 to 1.00 and the samples belong to Metalumious rock as shown in the diagram of the aluminum saturation index diagram (Figure 6b). Most of the samples had high K2O contents (4.31–5.03%), and the samples were plotted into calcic–alkali field in the K2O+ Na2O–CaO VS SiO2 diagram (Figure 6c). A low MgO content (0.40–0.59%) and high FeOt/(FeOt + MgO) ratio (0.80–0.82) indicate that the rocks are rich in iron (Figure 6d).

Table 2

Analyzed data of major, rare earth and trace elements of Haobugao granites

Sample H-08 H-09 H-10 H-11 H-12 Sample H-08 H-09 H-10 H-11 H-12
Al2O3 (wt%) 13.51 13.98 13.42 13.64 14.13 In 0.05 0.06 0.1 0.1 0.1
SiO2 71.46 72.17 73.19 71.25 70.75 Cs 7.18 6.02 6.5 4.6 6.0
CaO 1.58 1.42 1.74 2.16 1.89 Ba 245.08 258.42 247.0 339.4 340.8
K2O 4.25 4.14 3.69 4.60 4.40 La 24.57 25.08 36.3 21.5 24.8
Fe2O3 2.04 2.03 2.53 1.78 1.89 Ce 58.39 57.09 78.2 57.3 56.0
FeO 1.58 1.56 1.90 1.28 1.38 Pr 6.88 6.52 8.6 6.7 6.3
MgO 0.43 0.40 0.59 0.40 0.40 Nd 28.38 27.11 34.1 28.9 26.6
MnO 0.05 0.04 0.06 0.06 0.05 Sm 6.67 6.13 7.0 6.7 5.8
Na2O 3.93 4.23 4.28 3.98 4.25 Eu 0.40 0.42 0.4 0.5 0.5
P2O5 0.08 0.07 0.10 0.09 0.07 Gd 6.11 5.43 6.6 5.8 5.1
TiO2 0.27 0.25 0.33 0.32 0.24 Tb 1.20 1.01 1.2 1.1 0.9
LOI 1.67 1.58 0.73 1.48 1.48 Dy 7.60 6.60 7.3 6.9 5.9
Total 99.24 100.3 100.66 99.75 99.55 Ho 1.60 1.44 1.6 1.5 1.2
DI 86.96 87.52 85.49 87.02 87 Er 4.62 4.29 4.5 4.3 3.6
SI 3.5 3.21 4.54 3.34 3.24 Tm 0.79 0.75 0.8 0.7 0.6
A/CNK 0.97 0.998 0.946 0.882 0.93 Yb 5.21 4.89 5.0 4.5 3.8
A/NK 1.22 1.22 1.22 1.18 1.20 Lu 0.80 0.77 0.8 0.7 0.6
Li (ppm) 21.69 19.57 12.8 11.5 15.3 Hf 5.52 6.05 6.9 4.7 4.6
Be 5.49 5.87 6.1 6.0 5.2 Ta 2.41 2.51 2.2 2.3 1.8
Sc 3.95 3.62 5.2 4.7 4.1 W 16.88 10.79 2.5 4.8 9.1
V 16.03 15.63 20.7 20.4 16.9 Tl 1.09 0.94 1.1 0.8 1.1
Co 2.51 2.35 3.2 2.7 2.4 Pb 16.78 16.98 18.6 17.8 22.1
Ni 3.20 3.77 15.7 18.2 2.2 Bi 0.12 0.07 0.1 0.1 0.1
Cu 3.40 3.10 7.8 4.1 4.0 Th 27.95 28.89 38.4 35.5 24.2
Zn 52.75 57.46 97.3 50.0 59.5 U 13.05 15.35 11.9 11.3 8.2
Ga 20.90 21.52 21.8 20.7 21.1 ΣREE 153.22 147.54 192.44 147.17 141.71
As 0.66 0.65 0.7 0.6 0.7 LREE 125.29 122.35 164.71 121.65 120.04
Sr 147.30 159.56 192.9 206.9 197.6 HREE 27.93 25.19 27.73 25.53 21.68
Y 45.60 41.91 44.1 42.3 35.0 LR/HR 4.49 4.86 5.94 4.77 5.54
Zr 145.95 146.09 191.0 128.5 127.1 LaN/YbN 3.19 3.46 4.95 3.22 4.40
Nb 18.69 16.14 19.2 18.3 13.0 δEu 0.19 0.22 0.19 0.23 0.27
Mo 4.93 4.17 9.0 12.4 2.7 δCe 1.05 1.05 1.04 1.12 1.05
Cd 0.32 0.29 0.9 0.4 0.3
Figure 6 Major element geochemical plots for the Haobuga granites. (a) Na2O + K2O vs SiO2(wt%) (after Wilson [41]); (b) A/NK vs A/CNK [A/CNK = molar Al2O3/(CaO + K2O + Na2O); A/NK = molar Al2O3/(K2O + Na2O)] (after Maniar and Piccoli [42]); (c) K2O + Na2O-CaO vs SiO2(wt%) (after Frost et al. [37]); and (d) FeOt/(FeOt + MgO) vs SiO2(wt%) (after Frost et al. [37]).
Figure 6

Major element geochemical plots for the Haobuga granites. (a) Na2O + K2O vs SiO2(wt%) (after Wilson [41]); (b) A/NK vs A/CNK [A/CNK = molar Al2O3/(CaO + K2O + Na2O); A/NK = molar Al2O3/(K2O + Na2O)] (after Maniar and Piccoli [42]); (c) K2O + Na2O-CaO vs SiO2(wt%) (after Frost et al. [37]); and (d) FeOt/(FeOt + MgO) vs SiO2(wt%) (after Frost et al. [37]).

Samples have high rare earth element (REE) contents (141.7–192.4 ppm), asymmetrically right-inclined REE patterns with high LREE/HREE ratios (4.77–5.84), and LaN/YbN ratios (3.19–4.95) and remarkable negative anomalies (δEu = 0.19–0.27, with an average of 0.22) (Figure 7a and Table 2).

Figure 7 (a) Chondrite-normalized REE and (b) primitive-mantle-normalized trace-element diagrams for the Haobugao granites. Chondrite and primitive-mantle values are from Boynton [50] and Sun and McDonough [51], respectively.
Figure 7

(a) Chondrite-normalized REE and (b) primitive-mantle-normalized trace-element diagrams for the Haobugao granites. Chondrite and primitive-mantle values are from Boynton [50] and Sun and McDonough [51], respectively.

The primitive-mantle-normalized trace-element diagram shows Haobugao granites have significantly low Ba, Ti, and Sr, and very high Nb and Ta contents (Figure 7b). The 10,000 × Ga/Al ratios are 2.81–3.12, higher than the average of 2.60 for global A-type granites [35].

4.3 Zircon Hf isotopes

The 176Yb/177Hf and 176Lu/177Hf ratios of the zircon analysis points were 0.053820–0.086751 and 0.001479–0.002392, respectively, and the initial 176Hf/177Hf ratio was 0.282814–0.282940, corresponding to εHf(t) values of +5.62 to +9.12 and a T DM2 of 621–906 Ma (Table 3). The above-mentioned analyzed zircons have similar Hf isotope compositions to those of other Phanerozoic igneous rocks in the CAOB [36] (Figure 8a and b).

Table 3

In situ zircon Hf isotopic data for the Haobugao granites

No. 176Hf/177Hf 2σ 176Lu/177Hf 176Yb/177Hf Age (Ma) ε Hf (0) ε Hf(t) T DM1 T DM2 f Lu/Hf
1 0.002085 0.079753 0.282906 0.000016 152.8 4.73 7.88 505 699 −0.94
2 0.001997 0.069797 0.282940 0.000015 152.8 5.95 9.12 454 621 −0.94
3 0.001905 0.065879 0.282879 0.000020 152.8 3.80 6.96 541 758 −0.94
6 0.002392 0.086751 0.282889 0.000016 152.8 4.13 7.25 535 741 −0.93
7 0.002263 0.078693 0.282901 0.000015 152.8 4.55 7.67 515 712 −0.93
9 0.001707 0.059501 0.282890 0.000015 152.8 4.17 7.35 523 733 −0.95
10 0.001785 0.068139 0.282814 0.000023 152.8 1.49 4.66 634 906 −0.95
11 0.001479 0.053820 0.282867 0.000014 152.8 3.37 6.57 553 784 −0.96
12 0.001840 0.064498 0.282866 0.000017 152.8 3.31 6.47 560 789 −0.94
14 0.002011 0.071501 0.282867 0.000015 152.8 3.36 6.50 561 788 −0.94
15 0.001939 0.068930 0.282887 0.000013 152.8 4.07 7.25 530 741 −0.94
16 0.001944 0.069227 0.282842 0.000019 152.8 2.47 5.62 596 843 −0.94
17 0.002145 0.078092 0.282915 0.000016 152.8 5.04 8.17 493 680 −0.94
18 0.001852 0.071322 0.282895 0.000012 152.8 4.34 7.49 518 723 −0.94
19 0.001670 0.058069 0.282884 0.000013 152.8 3.98 7.18 530 745 −0.95
Figure 8 Correlations between the Hf isotopic compositions and the ages of zircons from the Haobugao granites. CAOB – Central Asian Orogenic Belt; YFTB – Yanshan Fold and Thrust Belt (after Yang et al. [36]).
Figure 8

Correlations between the Hf isotopic compositions and the ages of zircons from the Haobugao granites. CAOB – Central Asian Orogenic Belt; YFTB – Yanshan Fold and Thrust Belt (after Yang et al. [36]).

5 Discussion

5.1 Petrogenesis of the Haobugao granites

Granitoids are traditionally classified into I, S, M, or A types based on their source and geochemical characteristics. The characteristics of Haobugao granites, with SiO2 contents of >72 wt% and A/CNK values of <1 (Table 2), are consistent with A-type or highly fractionated I-type granite. However, it is difficult to differentiate A-type granites from highly fractionated I-type granites with high SiO2 contents of >72 wt% as the geochemical and mineralogical compositions converge for different types of granites [37]. For example, high Ga/Al ratio is suggested to be a feature of A-type granitoids, which Whalen et al. [35] used as a discrimination for A-type granitoids, but some highly differentiated I-type granites also have high 10,000 Ga/Al ratios [38,39].

Nevertheless, the following features indicate Haobugao granite as A-type granite rather than highly differentiated I-type granites:

  1. Potassium and Rb, Zr and Hf, Nb and Ta, and Y and Ho have similar geochemical behaviors, and their ratios are always invariant in a magmatic system [40]. When magma is differentiated, their ratios will become significantly smaller [39,43,44]. Therefore, the Zr/Hf and Nb/Ta ratios of the whole rock can indicate the degree of granitic crystallization differentiation [45]. The Haobugao granites have high Zr/Hf (24.2–27.7, with an average of 26.6) and Nb/Ta ratios (6.4–8.9, with an average of 7.7), which are different from highly differentiated granite, and accordant with those of typical A-type granites [46].

  2. Haobugao granite has a high SiO2 content (70.75–73.19%), relatively high Sr abundance (147.3 × 10−6–206.9 × 10−6), and moderate negative Eu anomaly (Eu/Eu* = 0.19–0.27), resembling to those of typical undifferentiated A-type granite [47,48]. Meanwhile, the ratios of some elements, such as Ca/Sr (64–78), Rb/Sr (1.09–1.62), and Rb/Ba (0.66–0.97), are also similar to characteristic A-type primary acid magma [49]. These geochemical characteristics show that the granite did not undergo a differentiation process.

  3. A-type granites are rich in potassium (K2O content 4–6% or higher) and SiO2 (usually >70%, most of them >75%); poor in Al2O3, Sr, Ba, Eu, Ti, and P; and have an apparent negative Eu anomaly in the REE distribution. The contents of K2O (3.69–4.59%), SiO2 (70.75–73.19%), and Al2O3 (13.42–14.13%), an obvious negative Eu anomaly in the chondrite standardized REE distribution diagram, and Sr, Ba, Eu, Ti, and P, with a severe deficit in the primitive mantle normalized trace-elements distribution diagram, all indicate that the Haobugao granite has the characteristics of A-type granite.

Eby [46] classified A-type granites into two subgroups, A1 and A2, as they have different chemical properties and are produced in different tectonic backgrounds. On the discriminant diagram of granite type, all of them fell into the range of A-type and A2-type granites (Figure 9). A1-type granites have similar chemical characteristics to oceanic island basalt [52] and are considered to be produced in an intraplate environment. By contrast, A2-type granites have a similar geochemical affinity to island arc basalt which are considered to be produced in a post-orogenic extension environment. A large amount of post-collision magmatism often marks the strong upwelling of the deep asthenosphere, especially the forming of A2-type granites under high temperature and low pressure [46]. Therefore, the identification of A2-type granites usually indicates an important geodynamic process – delamination in a post-collision extension setting [40,53,54,55,56,46].

Figure 9 (a) Zr vs 10,000 × Ga/Al and (b) FeOt/MgO vs 10,000 × Ga/Al diagrams showing the A-type signature of the Haobugao granites (after Whalen et al. [35]). (c) Nb-Y-Ce and (d) Nb-Y-3*Ga diagrams for subdividing A-type granite (after Eby [46]), indicating that the Haobugao granites belong to the A2-subgroup.
Figure 9

(a) Zr vs 10,000 × Ga/Al and (b) FeOt/MgO vs 10,000 × Ga/Al diagrams showing the A-type signature of the Haobugao granites (after Whalen et al. [35]). (c) Nb-Y-Ce and (d) Nb-Y-3*Ga diagrams for subdividing A-type granite (after Eby [46]), indicating that the Haobugao granites belong to the A2-subgroup.

Dall’Agnol and Oliveira [57] proposed that A-type granites could be divided into reduced and oxidized subtypes according to the redox state and water content in forming A-type granites. Reduced A-type granites are relatively anhydrous in their sources (2–3 wt%, H2O), probably derived from Q-feldspathic igneous sources and at a higher melting (>900°C) temperature. Oxidized A-type granite resources have appreciable water content (>4 wt%), at a relatively lower melting temperature and a lower crustal Q-feldspathic igneous source. The geochemical compositions of the samples are characterized by high whole-rock FeOT/(FeOT + MgO) values (>0.8), metaluminous and high K2O contents. Mineralogically, the Haobugao granites contain ferroan Bt. These geochemical and mineralogical characteristics are consistent with oxidized A-type granites and fall into the oxidized A-type granite field on the discrimination diagrams (Figure 10).

Figure 10 (a) FeOt/(FeOt + MgO) vs Al2O3 and (b) FeOt/(FeOt + MgO) vs Al2O3/(K2O/Na2O). Diagrams show the composition of representative oxidized and reduced A-type granites compared with calc-alkaline granites (after Dall’Agnol and Oliveira [57]).
Figure 10

(a) FeOt/(FeOt + MgO) vs Al2O3 and (b) FeOt/(FeOt + MgO) vs Al2O3/(K2O/Na2O). Diagrams show the composition of representative oxidized and reduced A-type granites compared with calc-alkaline granites (after Dall’Agnol and Oliveira [57]).

Although A-type granites are generally formed under extensional tectonic settings, there is no clear consensus on their origin [58]. A-type granite could have originated from the extreme crystallization differentiation of a mantle-derived basaltic melt [46], partial melting of crust-derived sources, or crust-mantle mixing [36,59].

High SiO2 contents, depleted in HFSE, enriched in LILE and LREE, low Mg*, and low compatible elements such as Cr, Ni, and Co contents indicate that mantle-derived materials were not significantly involved in their formation [60,61]. The limited variations in geochemical compositions, εHf(t) values in the Haobugao granites, exclude their formation from the crust-mantle mixing, as such a process would produce melts with scattered isotopic signatures [62,63].

A comparison of the average Nb/U and Ce/Pb ratios of the primitive mantle (30 and 9), OIB (47 ± 10 and 25 ± 5), and continental crust (10 and 4) [64] with the average values of 1.5 and 3.4 for the samples showed that Haobugao A-type granite has a closer affinity with crustal materials than primitive mantle values. Both the Zr/Hf ratios (24.2–27.7) and Nb/Ta ratios (6.4–8.9) are closer to crustal values (33 and 11.4, respectively) [65] than primitive mantle values (37 and 17.8, respectively) [66], indicating a crustal component in the source of the magmas. The Rb/Sr ratios (1.1–1.6), Ti/Y ratios (35.1–44.8), and Ti/Zr ratios (10.1–11.4) are also consistent with a continental crustal source. The zircon Hf isotope data further constrain the nature of the magma sources that all magmatic zircons have positive εHf(t) values (+5.6 to +9.1) and plot between the depleted mantle and CHUR lines in a ε Hf(t) versus time diagram. Their Hf two-stage model ages of 621–906 Ma suggests that the primary magmas were generated by partial melting of dominantly juvenile crustal material since Hf isotope compositions of the zircons are similar to those of the other Phanerozoic igneous rocks in the CAOB [15]. Thus, the magma of the Late Jurassic granites originated from the partial melting of the thickened juvenile lower crust.

5.2 Tectonic implications

Establishing the tectonic setting of Late Jurassic granites is important for understanding the evolution of CAOB and the geological development of NE China. Two distinct models have been proposed to explain the origin of the Jurassic magmatism in the Great Xing’an Range: (1) subduction of the Paleo-Pacific Plate beneath the eastern Asian continent [10,67,68,69] and (2) post-collision extension of Mongol–Okhotsk tectonic regime [29,70,71,72].

The widespread Jurassic accretionary complexes along the eastern margin of the Asian continent, together with an Early Jurassic N–S-trending magmatic arc and coeval mafic intrusions, I-type granitoids, and silicic lavas, which are subparallel to the Heilongjiang complex suggested that the Paleo-Pacific Plate was subducted beneath this margin in the Early Jurassic, and the following continuous subduction during the Jurassic, which resulted in crustal shortening and thickening, and widespread magmatism in NE China [30,73,74]. However, this mechanism cannot explain the Late Jurassic extension in the Great Xing’an Range, because Late Jurassic igneous rocks in NE China are comparatively rare in the Xing’an–Zhangguangcai ranges and the eastern parts of Jilin provinces and Heilongjiang [16], mainly within the Great Xing’an Range [75,76,77,78], which means that there was no subduction around the Pacific Ocean in Late Jurassic and precludes a relationship between the Jurassic igneous rocks and subduction of the Paleo-Pacific Plate.

Recent studies suggest a more possible genetic relationship between Jurassic volcanism in the Great Xing’an Range and the evolution of the Mongol–Okhotsk Ocean. First, the northern margin of the Mongolia–North China continent, along the southern margin of the Mongol–Okhotsk Ocean, was considered a passive margin from the late Permian onwards [11]. However, a recent study of Mesozoic calc-alkaline volcanic belts and intrusions along the southern margin of the Mongol–Okhotsk Suture Belt indicates southward subduction beneath the Erguna Massif [8,15]. Second, a Middle Jurassic muscovite granite (∼168 Ma) found from the Sunwu area in NE China indicates that the Mongol–Okhotsk Ocean to the northwest of the Erguna Massif was closed in the Middle Jurassic [79]. In addition, the ENE distribution of Late Jurassic volcanic rocks along the Mongol–Okhotsk Suture Belt in the western-most part of the Great Xing’an Range indicates their close relationship to this belt, rather than to the NE Paleo-Pacific margin [8].

Wang et al. [79] and Zhang et al. [80] reported the discovery of riebeckite rhyolites in the SGXR and suggested that these rhyolites formed in an environment of extensional lithosphere after the closure of Mongol–Okhotsk Ocean with a primary magma resulting from the partial melting of the ancient oceanic slab. Besides, Shang et al. [81] and Li et al. [78] found some adakitic intrusive rocks of the same period, which suggests that the lower crust of the Great Xing’an Range had been thickened in Middle-Late Jurassic. Our discovery of Haobugao A2-type granite further verifies the major role of oceanic plate in the formation of the Late Jurassic magmatic rocks. The geochemical characteristics of the Haobugao granites are similar to those of IAB (island arc basalt) (Figure 11a and b), which belong to post-orogenic granite. Rb, Nb, and Y indicate that Haobugao granites were formed in a post-orogenic environment (Figure 11c and d). Thus, Haobugao granites have an A2-subtype geochemical affinity, suggesting that the granites formed in a post-collisional setting [46], and the primary magma of the granite was probably derived from the partial melting of a delaminated region of the lower crust, an interpretation that is supported by the presence of Middle Jurassic thickened lower crust in the study area.

Figure 11 Discrimination diagrams for Haobugao granites in (a and b) after Dall’Agnol and Oliveira [57]; (c) after Pearce et al. [82]; and (d) after Pearce [83].
Figure 11

Discrimination diagrams for Haobugao granites in (a and b) after Dall’Agnol and Oliveira [57]; (c) after Pearce et al. [82]; and (d) after Pearce [83].

In summary, Haobugao A2-type granite indicates that Late Jurassic magmatism in the Xing’an Massif occurred in an extensional environment related to the collapse or delamination of a thickened region of the lithosphere after closure of the Mongol–Okhotsk Ocean.

6 Conclusion

  1. U–Pb zircon geochronology indicates a Late Jurassic age (152.7 ± 0.5 Ma) for Haobugao granites in the Xing’an Massif;

  2. The Haobugao granites have the geochemical signatures typical of A-type granite, with an affinity of the A2 subtype;

  3. The Late Jurassic granites in the Great Xing’an Range were formed in a post-collisional extensional setting. The gravitational collapse of the organically thickened crust was closely related to break-off of the subducted oceanic slab and upwelling of the asthenosphere after closure of the Mongol–Okhotsk Ocean.

Acknowledgments

The authors thank the Heilongjiang Natural Science Foundation project (TD2019D001) for providing financial support so that they can better carry out scientific research and learning.

  1. Conflict of interest: We declare that we do not have any commercial or associative interest that represents a conflict of interest in connection with the work submitted.

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Received: 2023-05-08
Revised: 2023-09-22
Accepted: 2023-10-14
Published Online: 2023-11-13

© 2023 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-2022-0567
Keywords for this article
Xing’an Massif; Late Jurassic; A2-type granites; petrogenesis; geochronology; geochemistry; Mongol–Okhotsk oceanic plate
Creative Commons
BY 4.0

Articles in the same Issue

  1. Regular Articles
  2. Diagenesis and evolution of deep tight reservoirs: A case study of the fourth member of Shahejie Formation (cg: 50.4-42 Ma) in Bozhong Sag
  3. Petrography and mineralogy of the Oligocene flysch in Ionian Zone, Albania: Implications for the evolution of sediment provenance and paleoenvironment
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  6. Carbonate texture identification using multi-layer perceptron neural network
  7. Metallogenic model of the Hongqiling Cu–Ni sulfide intrusions, Central Asian Orogenic Belt: Insight from long-period magnetotellurics
  8. Assessments of recent Global Geopotential Models based on GPS/levelling and gravity data along coastal zones of Egypt
  9. Accuracy assessment and improvement of SRTM, ASTER, FABDEM, and MERIT DEMs by polynomial and optimization algorithm: A case study (Khuzestan Province, Iran)
  10. Uncertainty assessment of 3D geological models based on spatial diffusion and merging model
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  18. A prediction model for Xiangyang Neolithic sites based on a random forest algorithm
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  63. Analysis of artificial intelligence approaches to predict the wall deflection induced by deep excavation
  64. Evaluation of the current in situ stress in the middle Permian Maokou Formation in the Longnüsi area of the central Sichuan Basin, China
  65. Utilizing microresistivity image logs to recognize conglomeratic channel architectural elements of Baikouquan Formation in slope of Mahu Sag
  66. Resistivity cutoff of low-resistivity and low-contrast pays in sandstone reservoirs from conventional well logs: A case of Paleogene Enping Formation in A-Oilfield, Pearl River Mouth Basin, South China Sea
  67. Examining the evacuation routes of the sister village program by using the ant colony optimization algorithm
  68. Spatial objects classification using machine learning and spatial walk algorithm
  69. Study on the stabilization mechanism of aeolian sandy soil formation by adding a natural soft rock
  70. Bump feature detection of the road surface based on the Bi-LSTM
  71. The origin and evolution of the ore-forming fluids at the Manondo-Choma gold prospect, Kirk range, southern Malawi
  72. A retrieval model of surface geochemistry composition based on remotely sensed data
  73. Exploring the spatial dynamics of cultural facilities based on multi-source data: A case study of Nanjing’s art institutions
  74. Study of pore-throat structure characteristics and fluid mobility of Chang 7 tight sandstone reservoir in Jiyuan area, Ordos Basin
  75. Study of fracturing fluid re-discharge based on percolation experiments and sampling tests – An example of Fuling shale gas Jiangdong block, China
  76. Impacts of marine cloud brightening scheme on climatic extremes in the Tibetan Plateau
  77. Ecological protection on the West Coast of Taiwan Strait under economic zone construction: A case study of land use in Yueqing
  78. The time-dependent deformation and damage constitutive model of rock based on dynamic disturbance tests
  79. Evaluation of spatial form of rural ecological landscape and vulnerability of water ecological environment based on analytic hierarchy process
  80. Fingerprint of magma mixture in the leucogranites: Spectroscopic and petrochemical approach, Kalebalta-Central Anatolia, Türkiye
  81. Principles of self-calibration and visual effects for digital camera distortion
  82. UAV-based doline mapping in Brazilian karst: A cave heritage protection reconnaissance
  83. Evaluation and low carbon ecological urban–rural planning and construction based on energy planning mechanism
  84. Modified non-local means: A novel denoising approach to process gravity field data
  85. A novel travel route planning method based on an ant colony optimization algorithm
  86. Effect of time-variant NDVI on landside susceptibility: A case study in Quang Ngai province, Vietnam
  87. Regional tectonic uplift indicated by geomorphological parameters in the Bahe River Basin, central China
  88. Computer information technology-based green excavation of tunnels in complex strata and technical decision of deformation control
  89. Spatial evolution of coastal environmental enterprises: An exploration of driving factors in Jiangsu Province
  90. A comparative assessment and geospatial simulation of three hydrological models in urban basins
  91. Aquaculture industry under the blue transformation in Jiangsu, China: Structure evolution and spatial agglomeration
  92. Quantitative and qualitative interpretation of community partitions by map overlaying and calculating the distribution of related geographical features
  93. Numerical investigation of gravity-grouted soil-nail pullout capacity in sand
  94. Analysis of heavy pollution weather in Shenyang City and numerical simulation of main pollutants
  95. Road cut slope stability analysis for static and dynamic (pseudo-static analysis) loading conditions
  96. Forest biomass assessment combining field inventorying and remote sensing data
  97. Late Jurassic Haobugao granites from the southern Great Xing’an Range, NE China: Implications for postcollision extension of the Mongol–Okhotsk Ocean
  98. Petrogenesis of the Sukadana Basalt based on petrology and whole rock geochemistry, Lampung, Indonesia: Geodynamic significances
  99. Numerical study on the group wall effect of nodular diaphragm wall foundation in high-rise buildings
  100. Water resources utilization and tourism environment assessment based on water footprint
  101. Geochemical evaluation of the carbonaceous shale associated with the Permian Mikambeni Formation of the Tuli Basin for potential gas generation, South Africa
  102. Detection and characterization of lineaments using gravity data in the south-west Cameroon zone: Hydrogeological implications
  103. Study on spatial pattern of tourism landscape resources in county cities of Yangtze River Economic Belt
  104. The effect of weathering on drillability of dolomites
  105. Noise masking of near-surface scattering (heterogeneities) on subsurface seismic reflectivity
  106. Query optimization-oriented lateral expansion method of distributed geological borehole database
  107. Petrogenesis of the Morobe Granodiorite and their shoshonitic mafic microgranular enclaves in Maramuni arc, Papua New Guinea
  108. Environmental health risk assessment of urban water sources based on fuzzy set theory
  109. Spatial distribution of urban basic education resources in Shanghai: Accessibility and supply-demand matching evaluation
  110. Spatiotemporal changes in land use and residential satisfaction in the Huai River-Gaoyou Lake Rim area
  111. Walkaway vertical seismic profiling first-arrival traveltime tomography with velocity structure constraints
  112. Study on the evaluation system and risk factor traceability of receiving water body
  113. Predicting copper-polymetallic deposits in Kalatag using the weight of evidence model and novel data sources
  114. Temporal dynamics of green urban areas in Romania. A comparison between spatial and statistical data
  115. Passenger flow forecast of tourist attraction based on MACBL in LBS big data environment
  116. Varying particle size selectivity of soil erosion along a cultivated catena
  117. Relationship between annual soil erosion and surface runoff in Wadi Hanifa sub-basins
  118. Influence of nappe structure on the Carboniferous volcanic reservoir in the middle of the Hongche Fault Zone, Junggar Basin, China
  119. Dynamic analysis of MSE wall subjected to surface vibration loading
  120. Pre-collisional architecture of the European distal margin: Inferences from the high-pressure continental units of central Corsica (France)
  121. The interrelation of natural diversity with tourism in Kosovo
  122. Assessment of geosites as a basis for geotourism development: A case study of the Toplica District, Serbia
  123. IG-YOLOv5-based underwater biological recognition and detection for marine protection
  124. Monitoring drought dynamics using remote sensing-based combined drought index in Ergene Basin, Türkiye
  125. Review Articles
  126. The actual state of the geodetic and cartographic resources and legislation in Poland
  127. Evaluation studies of the new mining projects
  128. Comparison and significance of grain size parameters of the Menyuan loess calculated using different methods
  129. Scientometric analysis of flood forecasting for Asia region and discussion on machine learning methods
  130. Rainfall-induced transportation embankment failure: A review
  131. Rapid Communication
  132. Branch fault discovered in Tangshan fault zone on the Kaiping-Guye boundary, North China
  133. Technical Note
  134. Introducing an intelligent multi-level retrieval method for mineral resource potential evaluation result data
  135. Erratum
  136. Erratum to “Forest cover assessment using remote-sensing techniques in Crete Island, Greece”
  137. Addendum
  138. The relationship between heat flow and seismicity in global tectonically active zones
  139. Commentary
  140. Improved entropy weight methods and their comparisons in evaluating the high-quality development of Qinghai, China
  141. Special Issue: Geoethics 2022 - Part II
  142. Loess and geotourism potential of the Braničevo District (NE Serbia): From overexploitation to paleoclimate interpretation
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