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Article

Zircon U-Pb Dating and Geological Significance of Late Paleozoic Intrusive Rocks in the Khanbogd-Erdene Area, Southern Mongolia

by
Chao Fu
1,2,3,*,
Jun-Jian Li
1,*,
Shuai Zhang
4,
Peng Ji
4,
Zhi-Cai Dang
2,
Si-Yuan Li
2 and
Naidansuren Tungalag
5
1
Tianjin Center, China Geological Survey (North China Center for Geoscience Innovation), Tianjin 300170, China
2
School of Earth Sciences and Resources, China University of Geosciences Beijing, Beijing 100083, China
3
College of Earth Science and Engineering, Shandong University of Science and Technology, Qingdao 266590, China
4
Mongolia Zhengyuan Co., Ltd., Ulaanbaatar 211238, Mongolia
5
Institute of Geology, Mongolian Academy of Sciences, Ulaanbaatar 211238, Mongolia
*
Authors to whom correspondence should be addressed.
Minerals 2025, 15(12), 1236; https://doi.org/10.3390/min15121236 (registering DOI)
Submission received: 30 September 2025 / Revised: 17 November 2025 / Accepted: 18 November 2025 / Published: 23 November 2025
(This article belongs to the Section Mineral Geochemistry and Geochronology)
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Abstract

The Khanbogd-Erdene region in southern Mongolia is a globally important copper–polymetallic metallogenic province, hosting large to super-large deposits, such as Oyu Tolgoi and Tsagaan Suvarga. The area experiences frequent tectonic–magmatic activity, particularly Late Paleozoic subduction-related magmatism, which controls the occurrence of large-scale copper–polymetallic mineralization. This study focuses on the Late Paleozoic granitic intrusive rocks in the Khanbogd-Erdene region of southern Mongolia. Using LA-ICP-MS and SHRIMP dating techniques, precise zircon U–Pb ages were obtained for 10 samples. A total of 209 zircon grains from these 10 intrusive rocks were analyzed, with most cathodoluminescence (CL) images of zircon grains showing distinct oscillatory zoning. Th/U ratios ranging from 0.11 to 2.92 indicate they are magmatic. The younger group of granitic rocks yielded ages between 260.2 ± 1.2 Ma and 286.6 ± 0.9 Ma, indicating an Early Permian geological age. The other seven samples yielded older ages between 315.9 ± 1.8 Ma and 340.9 ± 0.9 Ma, indicating a Carboniferous geological age. These large-scale Carboniferous to Early Permian intrusive rocks in the Khanbogd-Erdene region are products of tectonic–magmatic activity during specific stages of crustal evolution. The findings provide reliable chronological data for regional tectonic–magmatic activity and offer new evidence for constraining the timing of the Variscan orogeny in southern Mongolia.

1. Introduction

The Khanbogd-Erdene region in southern Mongolia, adjacent to China (Figure 1), is a globally significant copper–polymetallic metallogenic province and one of the world’s three major porphyry copper metallogenic belts [1,2,3,4,5,6,7,8]. The area has experienced frequent tectonic events that induced intensive magmatism with ages ranging from the Neoarchean to the Late Mesozoic, predominantly composed of granitic rocks that mostly occur as plutonic batholiths or small- to medium-sized stocks [9,10,11,12]. Among those, Late Paleozoic magmatism represented the most intensive magmatic activity in the Khanbogd-Erdene district, constituting the main body of the magmatic rock belt in the Khanbogd-Erdene region. More importantly, the Late Paleozoic magmatism shows a close spatial relationship and has been considered to have governed the formation of abundant critical metal deposits, including copper, gold, molybdenum, tungsten, tin, and silver–lead–zinc [13,14,15,16,17], such as the world-class Oyu Tolgoi porphyry copper–gold deposit [18,19,20,21] and the giant Tsagaan Suvarga porphyry copper–molybdenum deposit [22,23,24,25] (Figure 1c). Based on Sino-Mongolian international geoscientific cooperation, this study focuses on the Late Paleozoic granites in the Khanbogd-Erdene region of southern Mongolia. This study obtained new robust ages for ten intrusive massifs employing high-precision zircon U–Pb dating techniques (LA–ICP–MS and SHRIMP). These results establish a refined geochronological framework for Late Paleozoic magmatism, thereby providing critical constraints on the Late Paleozoic tectonic–magmatic evolution of the region and providing new insights into the timing of the Variscan orogeny in southern Mongolia. Furthermore, the precise dating of these intrusions allows us to investigate potential relationships between specific magmatic pulses and mineralization events.

2. Geological Background

The Khanbogd-Erdene region in southern Mongolia is situated at the intersection of the Baruun Urt-Hutag Uul-Dong Ujimqin-Arxan arc-basin belt and the Sulinheer-Mandula-Holingol arc-basin belt [9]. Within Mongolia, this area corresponds to the Hutag Uul and Baruun Urt terranes as defined by Professor Tomurtogoo [26]. The Baruun Urt–Hutag Uul–Dong Ujimqin–Arxan arc-basin belt is mainly composed of Early Paleozoic island arcs and back-arc basins, Late Paleozoic island arcs and back-arc basins, and Neoproterozoic island arcs [27]. The Early Paleozoic island arcs were developed in an active continental margin setting and consist of Early–Middle Silurian volcanic–sedimentary sequences. The Early Paleozoic back-arc basins, also formed in an active continental margin environment, comprise Early Cambrian to Ordovician–Late Silurian carbonate rocks and continental marginal clastic deposits [27,28]. The Late Paleozoic island arcs originated in a Late Paleozoic active continental margin setting and are composed of Early Devonian–Early Carboniferous intermediate volcanic rocks and carbonate formations [9]. The Late Paleozoic back-arc basins, likewise formed in an active continental margin environment, are represented by Early Devonian–Late Carboniferous carbonate rocks and terrigenous clastic sequences. The Neoproterozoic island arcs, developed in an active continental margin setting, are characterized by dismembered ophiolite suites and Neoproterozoic basalt–andesite formations [27,28]. The Sulinheer–Mandula–Holingol arc-basin belt primarily consists of Early Paleozoic island arcs and foreland basins, Late Paleozoic island arcs, back-arc basins, and foreland basins, as well as Early Paleozoic accretionary wedges and Paleoproterozoic uplifts. Within Mongolian territory, this belt includes the Sulinheer–Mandula–Holingol Late Paleozoic island arc, the Sulinheer–Mandula–Holingol Late Paleozoic back-arc basin, and the Duulgant–Ganqimaodu Early Paleozoic accretionary wedge. The Sulinheer–Mandula–Holingol Late Paleozoic island arc formed in an active continental margin setting as a thrust nappe complex, consisting of ophiolite fragments devoid of dyke intrusions and carbonate–volcanic mélanges that preserve Tethyan-type Early Paleozoic fossil remnants [29]. The Sulinheer–Mandula–Holingol Late Paleozoic back-arc basin, situated in the southwestern part of the Hutag Uul terrane of Mongolia, is represented by Late Carboniferous–Middle Permian continental marginal clastic formations. The Duulgant–Ganqimaodu Early Paleozoic accretionary wedge extends in an approximately E–W trend along the southern border region of Mongolia, where it connects with China’s Ganqimaodu area and consists of Ordovician greenschist formations.
In recent years, significant exploration breakthroughs have been made in copper–gold deposits in the Khanbogd-Erdene region, with newly discovered copper–gold deposits primarily associated with plutonic intrusive rocks. Large areas of intermediate–acidic intrusive rocks are developed along both sides of the fault zone, including lithologies such as granite, granodiorite, monzogranite, syenogranite, and minor basic–ultrabasic rocks. This subduction-related magmatism persisted from the Devonian and Carboniferous through to the Permian to Early Triassic [30,31,32], playing a crucial role in the formation of copper–polymetallic deposits. This study selects 10 intrusive rock bodies in the Khanbogd-Erdene region as research subjects (Figure 1): Sample (M7-9-3) is medium-coarse-grained granite, coordinates 111°05′15″ E, 44°13′54″ N; Sample (M7-9-4) is medium-fine-grained granite, coordinates 111°06′34″ E, 44°11′10″ N; Sample (M7-9-6) is medium-coarse-grained granite, coordinates 111°02′09″ E, 44°04′28″ N; Sample (M7-9-9) is medium-coarse-grained granite, coordinates 111°19′45″ E, 43°43′28″ N; Sample (M7-10) is fine-grained K-feldspar granite, coordinates 110°56′40″ E, 43°41′59″ N; Sample (M7-13-4) is medium-fine-grained granite, coordinates 108°47′27″ E, 42°32′40″ N; Sample (M7-14) is fine-grained granite, coordinates 109°40′17″ E, 42°34′23″ N; Sample (M9-3) is coarse-grained granite, coordinates 106°40′53″ E, 43°01′26″ N; Sample (M9-4) is medium-fine-grained monzogranite, coordinates 106°43′17″ E, 42°55′10″ N; and Sample (M9-5) is fine-grained syenogranite, coordinates 106°47′26″ E, 42°49′17″ N.

3. Analytical Methods

Zircon separation was conducted at the Langfang Regional Geological Survey Institute in Hebei Province using flotation and electromagnetic separation methods. Zircon grains with well-developed crystal forms and good transparency were selected under a binocular microscope, mounted on epoxy resin, and polished to create grain mounts. These mounts were then subjected to transmitted light, reflected light, and cathodoluminescence (CL) microscopic observation and imaging. For the majority of our samples, the zircon grains were of sufficient size to be effectively analyzed using LA-ICP-MS. However, for sample M7-9-4, some zircon grains were too small to use LA-ICP-MS to guarantee data quality. As such, we use the SHRIMP technique, which possesses superior spatial resolution, for M7-9-4 in this context.
The LA−ICP−MS zircon U−Pb testing was completed at the Isotope Laboratory of the Tianjin Center of Geological Survey. The experimental instrumentation utilized a Laser Ablation Multi-Collector Inductively Coupled Plasma Mass Spectrometer (LA-MC-ICP-MS), specifically comprising a Neptune multi-collector ICP-MS from Thermo Fisher Scientific and a NEW WAVE 193 nm FX ArF excimer laser from ESI. During the experimental procedure, a 193 nm laser was used to ablate the zircon samples and conduct in situ U−Pb isotope determination. The laser ablation spot size was set to 35 μm. Zircon standard 91,500, which has a 206Pb/238U age of 1065 ± 0.6 Ma, was used to calibrate the mass discrimination and isotope fractionation. Zircon standard GJ-1 was used as an unknown for verification of data quality. Common lead was corrected based on 208Pb, and the NIST SRM 610 glass standard was used as an external standard to calculate the U and Pb concentrations in the zircon samples. Data and diagram processing were performed using the ICP−MS DataCal program [33] and the Isoplot program [34].
The SHRIMP zircon U-Pb dating was completed at the Beijing SHRIMP Center. The SHRIMP standard used was TEMORAl zircon, with a 206Pb/238U ratio of 0.0668, corresponding to an age of 417 Ma. The standard index was 2.00, and the standard 207Pb/206Pb ratio was 0.551. The standard was analyzed once after every 2–4 measurements of unknown-age zircon grains. Data analysis and processing methods followed those described by Claesson et al. [35] and Compston et al. [36]. Age calculations employed the decay constants recommended by Steiger et al. [37].

4. Results

4.1. Zircon Cathodoluminescence (CL) Characteristics

Cathodoluminescence (CL) imaging (Figure 2 and Figure 3) reveals that the zircon grains predominantly exhibit elongated prismatic, short prismatic, and irregular subangular morphologies, displaying euhedral to subhedral crystal forms with particle sizes ranging from 90 to 200 μm. Most zircon grains show distinct oscillatory zoning, indicative of primary magmatic origin. Some grains exhibit core-rim structures, with a few displaying weakened zoning at the rims and signs of hydrothermal alteration. A total of 209 zircon grains from 10 samples were analyzed. For sample M7-9-4, the Th/U ratios range from 0.31 to 1.41, while those from the other nine samples vary between 0.11 and 2.92. These values exceed the critical thresholds of 0.1 or 0.4 [38,39,40], and the hydrothermal activity did not compromise the closed-system behavior of the U-Pb isotopic system in zircon, demonstrating typical magmatic zircon characteristics.

4.2. Zircon U−Pb Dating Results

Based on preliminary selection using zircon cathodoluminescence images, measurement spots were carefully positioned to avoid internal fractures and inclusions. A total of 209 zircon grains were selected for in situ analysis (Figure 4, Appendix A Table A1, Appendix A Table A2), with most measurement points located on distinct magmatic zoning. The primary criteria for excluding analyses from the weighted age calculation are as follows: (1) High Discordance: Analyses that have significant discordance (>10) are excluded, as this may indicate Pb-loss or mixing of age domains; (2) High Analytical Uncertainty: Analyses with exceptionally large uncertainties are scrutinized and may be excluded if they are statistical outliers that disproportionately inflate the overall uncertainty; (3) Presence of Inherited Core or Metamorphic Overprint: We use Cathodoluminescence (CL) images and dating results to guide our calculation so that the different age populations (e.g., inherited core) are excluded from the calculation of the magmatic crystallization age.
Sample (M7-9-3) yielded 206Pb/238U ages ranging from 317 ± 4 Ma to 359 ± 4 Ma, with a weighted mean age of 329.5 ± 1.9 Ma (after excluding grains #1, #3, #11, #12, #14, #16, #17, and #18, MSWD = 1.8, n = 12, 95% conf.). The Th/U ratios range from 0.85 to 2.94. Sample (M7-9-4) yielded 206Pb/238U ages ranging from 325.2 ± 3.6 Ma to 338.5 ± 2.4 Ma, with a weighted mean age of 331.6 ± 1.4 Ma (after excluding grain #8, MSWD = 0.33, n = 13, 95% conf.). The Th/U ratios range from 0.31 to 1.41. Sample (M7-9-6) yielded 206Pb/238U ages ranging from 326 ± 4 Ma to 342 ± 10 Ma, with a weighted mean age of 334.3 ± 1.9 Ma (MSWD = 0.86, n = 19, 95% conf.). The Th/U ratios range from 0.40 to 0.90. Sample (M7-9-9) yielded 206Pb/238U ages ranging from 267 ± 4 Ma to 285 ± 2 Ma, with a weighted mean age of 275.4 ± 1.7 Ma (MSWD = 2.7, n = 27, 95% conf.). The Th/U ratios range from 0.11 to 0.59. Sample (M7-10) yielded 206Pb/238U ages ranging from 268 ± 1 Ma to 283 ± 2 Ma, with a weighted mean age of 273.1 ± 0.6 Ma (after excluding grain #26, MSWD = 3.9, n = 25, 95% conf.). The Th/U ratios range from 0.45 to 0.66. Sample (M7-13-4) yielded 206Pb/238U ages ranging from 240 ± 3 Ma to 273 ± 3 Ma, with a weighted mean age of 263.2 ± 1.4 Ma (after excluding grains #9, #10, #15, #17, and #20, MSWD = 3.4, n = 15, 95% conf.). The Th/U ratios range from 0.40 to 0.85. Sample (M7-14) yielded 206Pb/238U ages ranging from 296 ± 3 Ma to 335 ± 4 Ma, with a weighted mean age of 316 ± 2 Ma (after excluding grains #1, #2, #3, #15, and #17, MSWD = 1.4, n = 13, 95% conf.). The Th/U ratios range from 0.25 to 1.05. Sample (M9-3) yielded 206Pb/238U ages ranging from 339 ± 2 Ma to 345 ± 2 Ma, with a weighted mean age of 340.9 ± 0.9 Ma (after excluding grain #21, MSWD = 0.53, n = 20, 95% conf.). The Th/U ratios range from 0.32 to 0.77. Sample (M9-4) yielded 206Pb/238U ages ranging from 334 ± 2 Ma to 335 ± 2 Ma, with a weighted mean age of 334.9 ± 1.3 Ma (after excluding grains #2, 4, 6, 7, 8, 10, 12, 13, 15, 16, and 19, MSWD = 0.052, n = 11, 95% conf.). The Th/U ratios range from 0.55 to 0.77. Sample (M9-5) yielded 206Pb/238U ages ranging from 285 ± 2 Ma to 288 ± 2 Ma, with a weighted mean age of 286.6 ± 0.9 Ma (after excluding grains #3, 4, 5, 6, 8, 10, 11, 12, 13, 16, and 22, MSWD = 0.36, n = 11, 95% conf.). The Th/U ratios range from 0.84 to 1.18.

5. Discussion

This study employs high-precision LA-ICP-MS and SHRIMP zircon U–Pb dating to determine the emplacement ages of ten intrusive massifs in the Khanbogd–Erdene region of southern Mongolia. Our results reveal two major episodes of magmatic activity: a Carboniferous phase (315.9 ± 1.8 Ma to 340.9 ± 0.9 Ma) and an Early Permian phase (260.2 ± 1.2 Ma to 286.6 ± 0.9 Ma). The findings illustrate multiple phases of tectono-magmatic activity in the Khanbogd–Erdene region, indicating that the southern Central Asian Orogenic Belt (CAOB) experienced at least two significant magmatic pulses during the Carboniferous and Early Permian, suggesting that mineralization in the area was not a single event, but rather a complex process linked to multiple tectonic–thermal events. The Carboniferous magmatism (ca. 316–341 Ma) is likely associated with the southward subduction of the Paleo-Asian Ocean plate beneath the North China Craton or other microcontinental blocks, leading to the formation of a subduction-related magmatic arc (e.g., [41,42]). In contrast, the Early Permian magmatism (ca. 260–287 Ma) likely marks a critical transition in the tectonic regime from compressional subduction-related orogenesis to a post-collisional or post-orogenic extensional setting (e.g., [12]). Such tectonic transitions often trigger crustal decompression melting and asthenospheric upwelling, creating highly favorable conditions for the development of large-scale ore-forming fluid systems and mineral deposits (e.g., [43]). The establishment of this high-precision geochronological framework significantly enhances our understanding of the tectono-magmatic processes along the southern margin of the CAOB and provides robust geochronological constraints for future mineral exploration targeting in this region.
In combination with previous geochronological and petrological studies [27,30,44], this study demonstrated that the subduction-related magmatism in the Khanbogd–Erdene region was prolonged, persisting from the Devonian to the Permian. This protracted magmatic activity corresponded to a series of tectonic regimes, including Devonian subduction, Early Carboniferous subduction–collision, and the development of the Paleozoic Andean-type magmatic island arc, and subsequent Mesozoic collisional and post-collisional events [27,30,44]. These multiphase and compositionally diverse magmatic events have directly controlled the formation of a variety of deposits, with porphyry mineralization being the dominant type [4,5,6,7,8]. Gerel et al. suggested that the Early Paleozoic granites in the Khanbogd-Erdene area are I-type granites, exhibiting subduction-related characteristics, while the Late Paleozoic was dominated by Middle–Late Devonian intermediate–acidic volcanic arc magmatism, which controlled copper–gold mineralization [25]. Nie, F.J. et al. divided the regional crustal evolution and metallogenesis in southern Mongolia during the Late Paleozoic into two stages: the syn-orogenic stage from the Devonian to Early Permian, which formed volcanic rock-hosted Cu–Zn deposits, porphyry Cu (Au), and Cu (Mo) deposits, and the Middle–Late Permian post-orogenic stage with relatively weak mineralization [4]. Li, J.J. et al. compiled a 1:1,000,000 series of geological maps for the Sino–Mongolian border region, identifying six periods of porphyry deposit mineralization and proposing that the Oyu Tolgoi–Tsagaan Suvarga metallogenic belt in southern Mongolia extends westward to connect with the East Tianshan metallogenic belt in China [8]. Jiang, S.H. et al. systematically summarized the metallogenic patterns of copper deposits in Mongolia, classifying the southern Mongolia region as a porphyry Cu–Mo–Au metallogenic belt related to the Mongol–Okhotsk Ocean tectonic system, further subdivided into a Devonian VMS-type Cu–Zn metallogenic sub-belt, a Late Devonian porphyry Cu–Au–Mo metallogenic sub-belt, and a Carboniferous porphyry Cu–polymetallic metallogenic sub-belt. They suggested a close relationship between the evolution of the Paleo-Asian Ocean branches, the tectonic nature of the Zun-Bayan Fault, and the extension of the copper metallogenic belt [8]. Zhang Weibo et al. proposed that the Late Paleozoic crustal evolution in southern Mongolia experienced a south-to-north single subduction model, where the Paleo-Asian oceanic crust subducted northward at a relatively shallow angle, forming a series of intrusive rocks and associated porphyry deposits [45].
Based on the above results, we propose that the Paleozoic crustal evolution and copper metallogenic framework in the Khanbogd-Erdene area can be summarized as follows: During the Early Paleozoic, multiple episodes of plate subduction triggered large-scale tectonic–magmatic activities, resulting in the formation of thick marine volcanic–sedimentary sequences and intrusive rocks within the Mandalovoo-Gurvansayhan terrane, thereby forming an Early Paleozoic magmatic belt within the island arc. In the Late Paleozoic, the syn-orogenic stage represented the main metallogenic epoch for porphyry copper deposits. Subduction of the Paleo-Asian Ocean plate from the Early Devonian to Early Carboniferous induced intense magmatism, leading to the extensive development of Variscan intermediate–acidic volcanic rocks and granitoid intrusions. Concurrently, hydrothermal fluids associated with intermediate–acidic magmas interacted with country rocks through water–rock interaction, forming porphyry copper deposits such as Oyu Tolgoi and Tsagaan Suvarga.

6. Conclusions

Based on high-precision LA-ICP-MS and SHRIMP zircon U–Pb dating, this study identifies two major magmatic events in the Khanbogd–Erdene region of southern Mongolia: a Carboniferous event (315.9 ± 1.8 Ma to 340.9 ± 0.9 Ma) and an Early Permian event (260.2 ± 1.2 Ma to 286.6 ± 0.9 Ma). In combination with previous studies, the Carboniferous magmatism is interpreted to be related to a continental arc formed by the southward subduction of the Paleo-Asian Ocean, while the Early Permian magmatism likely marks a key transition in the tectonic regime from subduction-related compression to post-collisional extension. The Late Paleozoic syn-orogenic stage (Early Devonian to Early Carboniferous) represents the main epoch of porphyry copper mineralization. These high-precision geochronological data provide new constraints for understanding the tectono-magmatic evolution of the southern Central Asian Orogenic Belt (CAOB)

Author Contributions

Conceptualization, C.F.; sampling and experiments, C.F., S.Z., P.J. and N.T.; data analysis and figures, Z.-C.D. and S.-Y.L.; writing—original draft preparation, C.F. and J.-J.L.; writing—review and editing, C.F., J.-J.L. and S.-Y.L. All authors have read and agreed to the published version of the manuscript.

Funding

This work was financially supported by the National Key R&D Program of China (Grant 2022YFE0119900), Research Program of Ministry of Natural Resources (ZKKJ202404), the Deep Earth Probe and Mineral Resources Exploration-National Science and Technology Major Project (2024ZD1002205 and 2024ZD1001902-1), and the China Geological Survey Project (DD20221695-30 and DD202402015). We are grateful to Prof. Orolmaa, D., for his help during the field work in Southern Mongolia, as well as Prof. Tu Jiarun, Geng Jianzhen, and Wu Lei for their help during LA–MC–ICP–MS zircon U-Pb isotope and major and trace elements analyses.

Data Availability Statement

The original contributions presented in this study are included in the article. Further inquiries can be directed to the corresponding authors.

Conflicts of Interest

Authors Shuai Zhang and Peng Ji were employed by the Mongolia Zhengyuan Co., Ltd. The remaining authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Appendix A

Table A1. LA-ICP-MS U-Pb dating of zircons from representative granitoids in Southern Mongolia.
Table A1. LA-ICP-MS U-Pb dating of zircons from representative granitoids in Southern Mongolia.
SampleIsotopic CompositionsAges (Ma)Trace Elements
206Pb/238UErr% (1σ)207Pb/235UErr% (1σ)207Pb/206PbErr% (1σ)208Pb/232ThErr% (1σ)232Th/238U206Pb/238U1σ207Pb/235U1σU (ppm)Pb (ppm)
M7-9-3
MND09-3TW1-10.050431.20.37592.70.054062.70.01591.31.04541324731741218
MND09-3TW1-20.051971.10.38432.00.053632.00.015581.02.504803306327416614
MND09-3TW1-30.050661.20.395652.90.056633.00.014751.50.934893388319423915
MND09-3TW1-40.052221.20.383182.50.053212.50.015411.21.31613329732841138
MND09-3TW1-50.053651.20.409242.40.055322.40.016341.21.12956348733741007
MND09-3TW1-60.052751.10.395621.90.054391.90.01571.10.900143385331420813
MND09-3TW1-70.051761.10.377971.80.052951.80.015511.01.806613265325324518
MND09-3TW1-80.052241.10.387872.00.053842.00.015811.01.438393336328417112
MND09-3TW1-90.051681.10.379531.70.053261.70.015481.01.679913275325329422
MND09-3TW1-100.051541.10.389572.20.054812.20.015681.02.922523346324412711
MND09-3TW1-110.081141.10.669821.50.059871.50.024491.00.793145216503529929
MND09-3TW1-120.055631.10.423832.10.055252.10.016181.11.393333596349419414
MND09-3TW1-130.051771.10.381372.20.053422.20.015381.02.063013286325413010
MND09-3TW1-140.057331.20.452662.10.057262.20.015521.21.444013797359420115
MND09-3TW1-150.051311.10.407931.60.057651.60.015951.00.855883475323340225
MND09-3TW1-160.058831.20.523292.70.06452.70.017011.31.571364279369414111
MND09-3TW1-170.055121.10.406882.10.053532.10.015241.11.280293476346416812
MND09-3TW1-180.054361.30.418572.90.055843.00.016031.31.67931355934141098
MND09-3TW1-190.053121.10.404412.00.05522.00.015351.01.835633456334419014
MND09-3TW1-200.052721.10.39152.00.053852.00.015431.02.095233356331418214
M7-9-6
MND09-6TW1-10.05301.20.402910.60.05529.80.02987.70.779833343443745833
MND09-6TW1-20.05393.60.42276.40.05693.80.01938.40.4507338123582321512
MND09-6TW1-30.05332.80.40426.40.05504.30.02317.30.399633593452254960
MND09-6TW1-40.05411.40.42709.40.05728.30.02125.90.5183340536234615
MND09-6TW1-50.05402.50.41746.40.05604.30.02156.30.817033993542315014
MND09-6TW1-60.05442.90.40808.40.05447.00.02017.60.4737342103482923916
MND09-6TW1-70.05300.50.41263.60.05653.30.01971.50.495633323511316113
MND09-6TW1-80.05181.10.43254.90.06064.30.02105.50.404832643651829661713
MND09-6TW1-90.05391.90.40705.70.05484.70.02016.40.902933863472051037
MND09-6TW1-100.05301.40.42775.10.05864.10.02008.40.896033353621822913
MND09-6TW1-110.05322.50.40235.60.05484.10.02056.30.685233483431935824
MND09-6TW1-120.05400.90.40242.10.05401.60.02602.80.47003393344743442
MND09-6TW1-130.05300.90.40813.40.05582.70.01852.20.601133333481282779
MND09-6TW1-140.05432.40.41496.40.05545.30.01845.60.653634183522375378
MND09-6TW1-150.05311.90.42494.30.05803.40.02372.10.506933463601656439
MND09-6TW1-160.05381.00.42363.00.05722.40.02662.00.784733843591131225
MND09-6TW1-170.05331.20.42034.80.05723.80.02363.70.646633543571727124
MND09-6TW1-180.05371.30.40797.50.05516.80.03337.00.593133743482621316
MND09-6TW1-190.05201.30.43191.70.06021.50.01801.80.61423274365623020
M7-9-9
MND09-9TW1-10.04352.20.32754.50.05463.10.01613.10.348927562881321811
MND09-9TW1-20.04391.20.31102.10.05141.60.02494.10.12142773275663931
MND09-9TW1-30.04380.40.31366.60.05196.50.01706.50.5946276127718836
MND09-9TW1-40.04401.50.31983.30.05282.70.01806.80.529227842819935
MND09-9TW1-50.04413.10.30296.10.04983.60.01356.40.3856278926916535
MND09-9TW1-60.04371.20.30775.40.05114.70.01835.10.31612763272151096
MND09-9TW1-70.04400.60.29625.40.04895.00.01696.80.215727822641424916
MND09-9TW1-80.04441.30.29794.40.04863.80.01605.20.413428042651245224
MND09-9TW1-90.04441.20.30921.70.05051.30.01511.10.57602803274529317
MND09-9TW1-100.04422.90.29543.90.04853.20.01933.40.311427982631027416
MND09-9TW1-110.04422.10.30942.50.05081.70.01531.70.28022796274741927
MND09-9TW1-120.04342.80.31058.20.05196.90.02059.20.51922748275231825173
MND09-9TW1-130.04411.60.28663.80.04713.10.01641.60.227627842561027214
MND09-9TW1-140.04360.70.29433.40.04892.90.01471.30.38402752262923213
MND09-9TW1-150.04242.90.27945.40.04784.30.01505.30.108926882501330916
MND09-9TW1-160.04341.40.30142.10.05041.80.01651.80.15332744267627815
MND09-9TW1-170.04312.50.30041.60.05062.10.01594.40.1788272726741427
MND09-9TW1-180.04324.60.29078.30.04886.70.04067.70.2272273122592228114
MND09-9TW1-190.04471.40.29975.80.04865.10.01953.40.131928242661530918
MND09-9TW1-200.04280.40.30761.80.05211.60.01872.40.11542701272541923
MND09-9TW1-210.04381.20.30216.30.05005.90.02049.80.217927632681720614
MND09-9TW1-220.04221.40.29226.20.05025.50.01948.40.36102674260161288
MND09-9TW1-230.04391.70.31743.70.05243.10.01726.50.58212775280101449
MND09-9TW1-240.04411.00.31953.90.05253.30.01663.00.254227832821119510
MND09-9TW1-250.04391.00.31151.70.05141.50.01702.40.25802773275521611
MND09-9TW1-260.04520.80.30061.00.04820.70.01623.90.15332852267331816
MND09-9TW1-270.04313.00.29815.40.05023.30.01831.30.182127282651428214
M7-10
MND010TW1-10.04400.60.31311.70.05161.40.02310.80.60122782277526115
MND010TW1-20.04331.00.32582.50.05461.90.01660.70.57212733286724416
MND010TW1-30.04380.90.31562.80.05232.20.01520.50.61132773279823815
MND010TW1-40.04340.70.31194.00.05213.70.01562.20.454527422761124614
MND010TW1-50.04320.80.33752.60.05672.20.01520.80.46442732295837822
MND010TW1-60.04371.40.31222.20.05191.90.01601.00.50722764276624415
MND010TW1-70.04403.00.30964.20.05113.20.01732.50.513527882741221613
MND010TW1-80.04321.20.31851.90.05351.70.01541.40.57212733281532922
MND010TW1-90.04281.30.31833.70.05393.30.01996.50.597127032811025614
MND010TW1-100.04360.70.31475.30.05235.00.01818.10.542627622781529118
MND010TW1-110.04301.30.32065.00.05414.30.02008.30.654627132821421613
MND010TW1-120.04380.40.31593.60.05233.30.01686.30.659927712791032719
MND010TW1-130.04301.30.31252.50.05271.40.01511.90.53262784276724315
MND010TW1-140.04310.90.32518.50.05477.80.01887.30.527227222862418611
MND010TW1-150.04320.90.32842.00.05521.60.01541.70.60512723288625815
MND010TW1-160.04340.70.31771.40.05311.20.01601.20.5782274228041518
MND010TW1-170.04490.80.31271.50.05050.90.01540.90.54262832276418511
MND010TW1-180.04341.90.32093.50.05362.60.01323.90.582927452831029116
MND010TW1-190.04301.00.31782.80.05362.20.01591.50.59642713280826415
MND010TW1-200.04240.30.30953.20.05293.10.01452.00.54722681274919011
MND010TW1-210.04391.10.32124.60.05313.90.01513.00.58562773283131729
MND010TW1-220.04420.70.32121.50.05271.20.01520.90.52612792283419911
MND010TW1-230.04350.80.32604.60.05433.90.01653.10.531427522871316011
MND010TW1-240.04300.60.31062.30.05232.10.01500.50.58212722275620312
MND010TW1-250.04360.90.31864.60.05304.20.01745.60.598627522811334321
MND010TW1-260.06042.60.47642.10.05722.60.07476.60.744537810389834523
M7-13-4
MND13-4YP-1-10.04331.20.30522.80.05112.80.01321.70.453327072733924
MND13-4YP-1-20.04041.10.29101.70.05221.70.01241.10.54932594256346121
MND13-4YP-1-30.04331.10.31071.60.05201.60.01341.00.75332754273345623
MND13-4YP-1-40.04291.10.31341.50.05301.50.01321.10.40422774271395744
MND13-4YP-1-50.04261.10.30291.90.05161.90.01301.20.70492695269326013
MND13-4YP-1-60.04321.20.30542.50.05122.50.01271.60.5181271627331608
MND13-4YP-1-70.04021.10.28441.60.05131.60.01221.10.82862544254358128
MND13-4YP-1-80.04111.10.30802.00.05442.00.01311.30.48072735259328613
MND13-4YP-1-90.03961.10.28152.00.05162.00.01141.20.68242524250341319
MND13-4YP-1-100.03801.10.30041.70.05731.70.00941.20.48902674241356823
MND13-4YP-1-110.04181.10.29822.00.05172.00.01241.20.65232655264340219
MND13-4YP-1-120.04161.20.31332.10.05472.10.01281.40.4772277526232019
MND13-4YP-1-130.04221.10.30131.80.05181.90.01281.30.39622674266335816
MND13-4YP-1-140.04051.10.28691.80.05131.80.01221.20.51602564256342919
MND13-4YP-1-150.03791.10.28751.90.05501.90.01061.20.85302574240362228
MND13-4YP-1-160.04091.10.29071.90.05151.90.01181.20.75982594259331115
MND13-4YP-1-170.03891.10.27941.70.05211.70.01201.20.53222504246360126
MND13-4YP-1-180.04051.10.28511.80.05111.80.01201.20.82112554256340019
MND13-4YP-1-190.04071.10.28861.90.05141.90.01181.30.69752574257328913
MND13-4YP-1-200.03331.10.32631.60.07111.50.01151.10.63192874211286734
M7-14
MN14Y-010.27351.13.72931.40.09891.40.07600.91.59241578111558157730
MN14Y-020.05331.20.43472.40.05922.50.01651.60.430036673354996
MN14Y-030.07211.10.54861.60.05521.60.02211.00.70674446449530126
MN14Y-040.05091.10.39452.00.05622.00.01531.30.47923386320322713
MN14Y-050.05021.40.36034.60.05214.60.01552.50.6010312123164463
MN14Y-060.05011.30.36114.10.05224.20.01462.20.6322313113154432
MN14Y-070.04991.40.39634.30.05754.40.01593.50.3195339133144432
MN14Y-080.04941.20.36142.60.05302.70.01451.80.4291313731141026
MN14Y-090.04891.10.36762.10.05452.10.01441.11.0477318630831549
MN14Y-100.05051.30.37304.10.05354.20.01553.00.3455322113184422
MN14Y-110.04931.20.37612.90.05532.90.01521.80.453132483104754
MN14Y-120.05031.20.35923.00.05183.10.01531.80.516331283164734
MN14Y-130.05131.30.38734.20.05474.20.01963.20.2534332123234342
MN14Y-140.05111.10.38132.00.05412.10.01511.30.4894328632141599
MN14Y-150.04701.10.34781.90.05361.90.01411.10.66723035296329116
MN14Y-160.04981.20.39103.20.05703.30.01661.90.491033593134603
MN14Y-170.06431.10.52291.60.05901.60.01831.00.61604275401454340
MN14Y-180.04951.20.38512.60.05652.70.01521.50.636433173114805
M9-3
MND103TW1-10.05470.70.39650.70.05250.60.01610.40.38513442339253329
MND103TW1-20.05470.70.40010.80.05310.60.01510.50.45063432342355031
MND103TW1-30.05490.70.40492.20.05352.30.01530.70.6730345234581348
MND103TW1-40.05500.70.40161.10.05301.00.01510.40.76613452343431319
MND103TW1-50.05430.60.39721.10.05311.10.01290.80.53563412340436320
MND103TW1-60.05490.70.40041.40.05291.40.01480.70.71773442342520612
MND103TW1-70.05430.60.39371.00.05261.00.01320.40.55133412337435320
MND103TW1-80.05440.80.39720.90.05290.70.01430.20.70343423340341624
MND103TW1-90.05420.60.39571.00.05300.90.01300.40.56913402339337721
MND103TW1-100.05410.60.39711.60.05321.60.01310.60.62723402340620211
MND103TW1-110.05420.60.39651.00.05310.90.01280.30.54803402339339522
MND103TW1-120.05440.60.39801.00.05301.00.01270.40.44993422340338221
MND103TW1-130.05440.60.39620.60.05280.60.01270.30.41663412339282345
MND103TW1-140.05440.60.39121.00.05220.90.01310.30.51353412335346226
MND103TW1-150.05410.60.39651.20.05321.20.01260.50.54303402339479144
MND103TW1-160.05400.60.39691.50.05331.50.01290.60.31693392339544123
MND103TW1-170.05440.60.40020.70.05330.70.01320.30.44083422342355030
MND103TW1-180.05440.60.40011.10.05331.00.01290.50.40673412342448526
MND103TW1-190.05410.60.39831.20.05331.20.01300.20.06283402340437619
MND103TW1-200.05430.60.39641.50.05291.40.01180.70.51383412339534319
MND103TW1-210.05250.60.38511.80.05321.80.01280.41.29333302331638624
M9-4
MND104TW1-10.05340.80.38803.20.05273.10.01530.80.7628335333311946
MND104TW1-20.05320.80.53392.50.07281.90.01902.30.458933434341123613
MND104TW1-30.05330.80.38854.30.05293.90.01451.70.7661335333314935
MND104TW1-40.05320.70.48624.20.06634.00.01632.00.7965334240217915
MND104TW1-50.05340.70.38821.30.05281.20.01400.50.73483352333425114
MND104TW1-60.05321.00.51721.20.07051.30.01740.60.51123343423529317
MND104TW1-70.05320.70.77372.60.10542.30.02292.90.65103342582151027
MND104TW1-80.05310.80.44151.60.06031.50.01390.80.67353343371624514
MND104TW1-90.05320.60.39062.60.05322.50.01290.80.71803342335920011
MND104TW1-100.05321.00.55212.50.07532.30.01691.10.6126334344611966
MND104TW1-110.05340.70.38881.30.05281.40.01430.90.69663352333421512
MND104TW1-120.05320.60.60432.30.08242.20.01860.80.61443342480111368
MND104TW1-130.05320.80.47992.40.06542.20.01531.20.71963343398101237
MND104TW1-140.05340.60.38962.00.05302.00.01460.70.58473352334717510
MND104TW1-150.05330.70.50781.20.06921.10.01560.60.83983342417524915
MND104TW1-160.05320.80.61131.30.08331.40.01960.60.3169334348461579
MND104TW1-170.05330.60.38952.70.05302.60.01420.90.69543352334916810
MND104TW1-180.05340.60.38991.90.05291.80.01450.70.7654335233461348
MND104TW1-190.05130.60.37561.60.05311.60.01381.10.06283232324530615
MND104TW1-200.05330.60.39071.60.05321.50.01440.50.66363342335518110
MND104TW1-210.05330.70.38991.90.05301.70.01490.60.67613352334617710
MND104TW1-220.05340.70.38971.50.05291.50.01680.60.55193352334524114
M9-5
MND105TW1-10.04520.60.32561.50.05221.50.01100.31.10152852286425213
MND105TW1-20.04550.50.32672.50.05202.40.01000.71.07602872287727314
MND105TW1-30.04890.70.56283.90.08353.90.01511.20.96853082453181438
MND105TW1-40.04540.50.41201.30.06581.30.01070.31.33392862350429716
MND105TW1-50.04540.60.49541.10.07921.00.01090.51.52622862409426115
MND105TW1-60.04540.60.54241.10.08660.80.01251.21.46582862440559035
MND105TW1-70.04540.60.31342.40.05002.40.01000.50.9604286227771558
MND105TW1-80.04540.60.79351.50.12671.40.04181.61.03492862593916514
MND105TW1-90.04540.50.32541.90.05201.80.01561.80.83572862286522112
MND105TW1-100.04540.80.44111.70.07051.80.01140.70.98122862371622912
MND105TW1-110.04540.60.66332.30.10592.50.01040.91.568028625171224714
MND105TW1-120.04540.70.81013.00.12952.80.02201.40.82802862603181429
MND105TW1-130.04530.60.61112.30.09792.30.01101.31.395628624841119511
MND105TW1-140.04550.60.32641.60.05201.70.01060.60.92252872287521211
MND105TW1-150.04550.60.32681.70.05211.70.01050.50.93602872287519710
MND105TW1-160.04540.60.42192.40.06742.30.01111.00.3169286235791919
MND105TW1-170.04520.60.32571.80.05231.70.01020.60.96242852286520410
MND105TW1-180.04580.60.32522.80.05152.80.01060.61.1580288228681226
MND105TW1-190.04570.70.32452.10.05152.10.01050.50.0628288228561767
MND105TW1-200.04550.60.32692.80.05222.80.01050.80.9518287228781457
MND105TW1-210.04570.60.32862.00.05222.00.01080.41.17542882288618710
MND105TW1-220.04430.50.37602.00.06162.00.00941.21.0351279232471658
Table A2. Shrimp U-Pb dating of zircons from the representative granitoids in Southern Mongolia.
Table A2. Shrimp U-Pb dating of zircons from the representative granitoids in Southern Mongolia.
SampleU
ppm		Th
ppm		Pb
ppm		232Th/238U206Pb/238UErr%
1σ		207Pb/226PbErr%
1σ		204Pb-Corrected U-Pb Isotopes204Pb-Corrected Ages (Ma)
206Pb */238UErr% (1σ)207Pb */
235U		Err% (1σ)207Pb */
206Pb *		Err% (1σ)206Pb/238U1σ207Pb/206Pb1σ
M7-9-4
1389115180.305218.970.670.060220.05230.70.385.10.05353282331114
2217210101.000618.740.860.06243.10.05290.90.415.90.0565.93323448131
3416229200.567618.240.640.09641.50.05260.90.4610.70.063113303714226
4500681231.405318.370.670.081581.20.05270.80.48.60.0568.63313433190
5995350.553818.561.30.07333.40.05291.40.4310.80.059113335575232
6520529241.050518.920.560.056251.70.05270.60.392.90.0532.8331233164
7369304170.849018.680.640.06021.90.05300.70.385.00.0524.93332303112
8691583310.871619.2680.430.10210.980.04960.60.459.20.0669.23122815192
9365424171.201618.580.780.06333.20.05310.90.387.60.0527.63333276174
10392221180.581619.10.640.05951.90.05200.70.386.00.05363272336136
11303140140.475518.390.70.06012.10.05390.70.44.70.0534.63392334105
12352171160.502518.750.660.06021.90.05290.70.395.00.0544.93322367111
13352400161.173818.570.80.06012.90.05340.80.45.60.0545.63363360126
14815789361.000019.261.10.056211.30.05171.10.382.70.0532.4325433355
Pb * represent rediogenic Pb.

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Minerals 15 01236 g001
Figure 1. Simplified tectonic map of Mongolia (a), simplified tectonic map of southern Mongolia (b), and distribution map of intrusive rocks in the Khanbogd-Erdene region (c).
Figure 1. Simplified tectonic map of Mongolia (a), simplified tectonic map of southern Mongolia (b), and distribution map of intrusive rocks in the Khanbogd-Erdene region (c).
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Figure 2. Cathodoluminescence (CL) images of zircons from intrusive rocks in the Khanbogd-Erdene region, southern Mongolia (samples M7-9-3, M7-9-4, M7-9-6, M7-9-9, and M7-10). The white scale bar is 100 μm.
Figure 2. Cathodoluminescence (CL) images of zircons from intrusive rocks in the Khanbogd-Erdene region, southern Mongolia (samples M7-9-3, M7-9-4, M7-9-6, M7-9-9, and M7-10). The white scale bar is 100 μm.
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Figure 3. Cathodoluminescence (CL) images of zircons from intrusive rocks in the Khanbogd-Erdene region, southern Mongolia (samples M7-13-4, M7-14, M9-3, M9-4, and M9-5). The white scale bar is 100 μm.
Figure 3. Cathodoluminescence (CL) images of zircons from intrusive rocks in the Khanbogd-Erdene region, southern Mongolia (samples M7-13-4, M7-14, M9-3, M9-4, and M9-5). The white scale bar is 100 μm.
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Figure 4. Zircon U−Pb concordia diagram for intrusive rocks from the Khanbogd-Erdene area, southern Mongolia.
Figure 4. Zircon U−Pb concordia diagram for intrusive rocks from the Khanbogd-Erdene area, southern Mongolia.
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MDPI and ACS Style

Fu, C.; Li, J.-J.; Zhang, S.; Ji, P.; Dang, Z.-C.; Li, S.-Y.; Tungalag, N. Zircon U-Pb Dating and Geological Significance of Late Paleozoic Intrusive Rocks in the Khanbogd-Erdene Area, Southern Mongolia. Minerals 2025, 15, 1236. https://doi.org/10.3390/min15121236

AMA Style

Fu C, Li J-J, Zhang S, Ji P, Dang Z-C, Li S-Y, Tungalag N. Zircon U-Pb Dating and Geological Significance of Late Paleozoic Intrusive Rocks in the Khanbogd-Erdene Area, Southern Mongolia. Minerals. 2025; 15(12):1236. https://doi.org/10.3390/min15121236

Chicago/Turabian Style

Fu, Chao, Jun-Jian Li, Shuai Zhang, Peng Ji, Zhi-Cai Dang, Si-Yuan Li, and Naidansuren Tungalag. 2025. "Zircon U-Pb Dating and Geological Significance of Late Paleozoic Intrusive Rocks in the Khanbogd-Erdene Area, Southern Mongolia" Minerals 15, no. 12: 1236. https://doi.org/10.3390/min15121236

APA Style

Fu, C., Li, J.-J., Zhang, S., Ji, P., Dang, Z.-C., Li, S.-Y., & Tungalag, N. (2025). Zircon U-Pb Dating and Geological Significance of Late Paleozoic Intrusive Rocks in the Khanbogd-Erdene Area, Southern Mongolia. Minerals, 15(12), 1236. https://doi.org/10.3390/min15121236

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