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Article

The Geochemical Characteristics, Genesis, and Geological Significance of Early Paleozoic Granites in the South Altun Orogenic Belt of Western China

by
Xu Zeng
1,2,3,*,
Suotang Fu
1,
Guiwen Wang
1,2,
Bo Wang
4,
Zhixiong Wu
4,
Haidong Cui
4 and
Zongqi Feng
5
1
College of Geosciences, China University of Petroleum, Beijing 102249, China
2
State Key Laboratory of Petroleum Resources and Prospecting, China University of Petroleum, Beijing 102249, China
3
PetroChina Research Institute of Exploration and Development, Langfang 065007, China
4
Research Institute of Oil Exploration and Development, Qinghai Oil Field Branch Company, China National Petroleum Corporation, Dunhuang 736202, China
5
Hebei Geological Survey and Mapping Institute, Space Information Technology Application Research Center of Hebei Bureau of Geology and Mineral Resources Exploration and Development, Langfang 065000, China
*
Author to whom correspondence should be addressed.
Appl. Sci. 2025, 15(22), 12239; https://doi.org/10.3390/app152212239
Submission received: 4 September 2025 / Revised: 8 November 2025 / Accepted: 15 November 2025 / Published: 18 November 2025
(This article belongs to the Special Issue Advances in Petroleum Exploration and Application)
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Abstract

The Altun Orogenic Belt (AOB) has undergone multiple complex subduction–collision events. However, there are numerous disagreements regarding the Early Paleozoic tectonic–magmatic evolution of the AOB, primarily due to differing interpretations of magmatic rock types and their sources. As a result, we conducted detailed geochemical analyses of granite samples obtained from several exploration wells in the Dongping area (DPA) of the South Altun Orogenic Belt (SAOB) at the western boundary of the Qaidam Basin. This approach differs from previous studies that mainly relied on outcrop samples. The granites in the study area are metaluminous and have high alkali contents (avg. 7.63%) and high TFe2O3/MgO ratios (avg. 4.50). Their rare-earth elements are enriched in light REEs and show weak to moderate negative Eu anomalies (δEu = 0.49–1.11). These geochemical signatures indicate an affinity to A-type granites. Through comprehensive diagram analysis, the rocks plot near the upper crustal composition in a Ta/Yb-Th/Yb diagram, indicating that they primarily originated from a mixed source of recycled and juvenile crustal material. A comprehensive analysis of the regional tectonic background shows that the Early Paleozoic granites in the SAOB formed in post-collisional extensional environments and syn-collisional volcanic arc tectonic settings. The majority formed in post-collisional extensional thinning environments, whereas a minority formed in syn-collisional volcanic arc tectonic settings, closely related to the subduction and collision of the Qaidam Block beneath the Central Altun Block.

1. Introduction

Granite is a primary constituent of the continental crust. It records information on the crust’s formation and development that significantly contributes to the study of continental dynamics [1]. The development of granite diversity and its continental dynamics are important scientific issues in studying granites. They can reveal the magmatic genesis associated with crustal subduction/folding. The SAOB has developed unique high-/ultrahigh-pressure metamorphic rocks and abundant granites throughout the Altun Mountains. The formation of these granites is closely related to continental crust subduction, exhumation, and orogenic collapse, providing insights into the study of the orogenic belt’s evolutionary history and deep crust–mantle interaction [2,3,4].
The SAOB has experienced multiple periods of subduction–collision events and initially formed during the Caledonian period of the Paleozoic era. It experienced early plate subduction–collision interactions, followed by strike–slip movements in the Mesozoic and Cenozoic eras, resulting in a composite orogenic belt composed of geological bodies formed in different periods and tectonic environments [5,6]. Many recent studies have investigated the SAOB, providing substantial progress. Based on comprehensive research results, previous studies have mainly focused on four stages of Early Paleozoic granite in the SAOB: the first-stage granite was formed between 483 and 462 Ma. The second-stage granite was formed between 456 and 442 Ma. The formation age of the third-stage granite is 436–419 Ma. The formation age of the fourth-stage granite is 411–403 Ma [4,7,8,9,10,11,12,13]. In addition, some Late Paleozoic granite bodies are exposed in the southern margin of the SAOB, such as the zircon U-Pb ages of the North Yigan medium coarse granodiorite, which are 352 ± 3 Ma, 349 ± 2 Ma, and 342 ± 2 Ma. Although there are some differences in the age of granite formation among different scholars, overall, the age is mainly concentrated between 483 and 400 Ma. It is worth noting that, based on age analysis, there are still many differences in the understanding of the Early Paleozoic tectonic magmatic evolution process of the SAOB among previous researchers [4,14]. Some scholars believe that the widely distributed Early Paleozoic granites in the SAOB, as well as Early Paleozoic Mg-Fe rocks coeval with these granites, formed during the tectonic–magmatic event related to the northward subduction of the South Altun Ocean. These scholars assume they are the product of partial melting of the subducted oceanic crust and the mixing with mantle materials [4,15,16]. Other scholars believe that the Early Paleozoic granites in the SAOB are primarily A-type granites, representing the extension stage after the uplift of the South Altun Mountains [12,13]. Wu et al. (2018) proposed that tectonic events, such as subduction, collision, and post-collision extension of the double ocean basins, were related to the South Altun Ocean and Middle Altun Ocean in the SAOB during the Early Paleozoic [14]. Some scholars have suggested that I-type granites are related to the northward subduction collision in the South Altun Ocean [2,4,12,13,14,16,17]. The early granites (490–460 Ma) in the South Altun area have the characteristics of island-arc granites and may be the product of crust–mantle interactions during oceanic crustal subduction [13]. In contrast, the middle granites (450–425 Ma) have the characteristics of syn-collisional granites [18], and the late granites (424–400 Ma) belong to the A2-type, which formed in a post-orogenic extensional environment [13,19].
Significant uncertainties exist regarding the spatial and temporal distribution of Paleozoic geochemical data, and the delineation and attribution of tectonic units in the AOB are highly controversial. We analyze the petrological and geochemical characteristics of Early Paleozoic granites in the Dongping area of the SAOB and investigate the plate convergence and collision relationship between the Qaidam Block and the Azhong Block to improve our understanding of Paleozoic magmatic and tectonic events in the AOB.

2. Geological Setting

The AOB is located on the northern margin of the Tibetan Plateau between the Tarim Block, Qaidam Block, and Qilian–Kunlun orogenic belt. Its strike is NEE, forming a division between the Qaidam Basin and the Tarim Basin [20]. It is an important subduction–collision mafic belt in NW China. The belt can be divided into five sub-tectonic units from north to south: the Northern Altun Terrane, Northern Altun Ophiolitic Mélange Belt, Central Altun Terrane, South Altun Ultrahigh Pressure Belt, and SAOMB [13,19,21] (Figure 1).
The South Altun ultrahigh-pressure belt and Southern Altun Ophiolitic Mélange Belt (SAOMB) are located south of the Altun fault. They are collectively known as the SAOB. The study area (DPA) is located in the eastern section of the SAOMB. The SAOMB is composed of basic–ultrabasic rocks and granites associated with basic volcanic rocks. The ultrabasic rocks are predominantly serpentinized peridotite, whereas the basic rocks are primarily hornblende and tholeiite basalt, forming an ophiolite association with siliceous rocks, biotite plagioclase gneisses, quartz schist, dolomitic marble, and other rocks [23]. In front of the South Altun Mountains, a series of arc-shaped mountains have formed, and the Dongping structure belt is one of them. The bedrock samples studied in this article were all collected from this nose structure belt. The Dongping structure belt is an ancient uplift that continued to develop after the Yanshan period [24]. The fission track and seismic profile of the phosphorite reveal that there were two major tectonic thermal movements after the Yanshan period, namely, 15–40 Ma and 15 Ma, which coincide with the activity time of the Altun Fault [25,26,27]. So, the DPA experiences frequent, intense, and large-scale magmatic activities characterized by multiple episodes and diverse types occurring in various tectonic environments.
Previous studies on Early Paleozoic granites in the AOB have proposed several interpretations concerning the magmatic activity and tectonic evolution. Wu (2014) studied the Mangya granite in the region and proposed that oceanic crust subduction occurred at around 460 Ma, with the area subsequently entering a post-collisional extensional stage due to stress relaxation between 411 and 404 Ma [28]. Dong (2011) investigated hornblende gabbro in the Mangya area and suggested that the South Altun region remained in an island-arc setting associated with oceanic crust subduction until about 444.9 Ma [29]. Kang (2016) divided the Early Paleozoic tectonic–magmatic evolution of South Altun into four stages: mid-ocean ridge spreading and oceanic crust subduction (>500 Ma), continental deep subduction during collisional orogeny (497–472 Ma), slab break-off (469–445 Ma), and post-collisional extension (424–385 Ma) [17]. Yang (2012) examined the Dimonilik granite in the SAOB and argued that the region underwent continental crustal thickening related to continent–continent collision at approximately 500 Ma and then entered an extensional stage following break-off of the subducted slab between 466 and 451 Ma [30]. Other researchers have analyzed the zircon U–Pb ages of Dongping granite and proposed that the SAOB remained in an oceanic crust subduction setting from 460 to 444 Ma. They further concluded that the “South Altun Ocean” closed at around 418 Ma, marking the beginning of intracontinental subduction and collisional orogeny [31,32].

3. Sample Collection and Experimental Analysis

Fifteen bedrock core samples were selected for the main element analysis, including three samples from the Well DP306, three samples from the Well DP5, two samples from Well DP7, two samples from Well DPH301, and the data of two samples from Well DP1H-2-3, which were sourced from [32]. Nine Dongping bedrock core samples were selected for trace element analysis, including three samples from DP306, two samples from Well DP7, and four samples from Well DP1H-2-3. The study area is predominantly composed of granite (Figure 2a–c,f) and monzogranite (Figure 2d,e). These rocks generally exhibit a massive structure with subhedral to euhedral mineral grains and consist mainly of quartz and feldspar, along with minor amounts of biotite and muscovite. Quartz commonly displays brittle deformation, while some feldspar grains have undergone sericitization and replacement by calcite. Biotite occurs interstitially between quartz and feldspar grains, with minor chloritization observed in some grains. Fractures in quartz and feldspar are typically filled with sericite and silica. Detailed core and microscopic observations were conducted. Major and trace element analyses were conducted after determining that the composition and structure of the samples had not undergone alteration, mineralization, or secondary weathering. A Bruker S2PUMA wavelength-dispersive X-ray fluorescence spectrometer was used for major element analysis. The experimental process follows the GB/T14506.28-2010 standard [33], and the analysis accuracy is better than 5%. An inductively coupled plasma mass spectrometer (ICP-MS) was used for trace element analysis of the samples dissolved in HF + HNO3. Among them, the analysis error of elements with trace element content greater than 10 × 10−6 is better than 5%, and the testing accuracy of elements with trace element content less than 10 × 10−6 is better than 10%. The specific analytical methods are described in Reference [29].

4. Geochemical Characteristics

4.1. Major Element Composition

Major and trace element analyses were conducted at the Gansu Provincial Key Laboratory of Petroleum Resources Research, affiliated with the Chinese Academy of Sciences. Major elements were determined using a Japan Scientific Corporation 3080E3 X-ray fluorescence spectrometer produced by Rigaku Corporation in Japan, with its origin in Osaka, Japan, Asia. Trace elements were analyzed by laser ablation, using an Agilent Technologies 7900 inductively coupled plasma mass spectrometer. The test results of the major element analysis of the granite samples are listed in Table 1. SiO2 has the highest content among the major elements, ranging from 69.94% to 75.19%, with an average of 72.29%. It is followed by Al2O3, with a content of 12.45% to 15.63%, averaging 14.19%. The K2O and Na2O contents range from 3.81% to 5.59% and 0.81% to 4.54%, respectively, with averages of 4.46% and 3.11%, while the content of K2O + Na2O is 5.82–8.73%, with an average of 7.57%. The content of Fe2O3 is 3.24–9.21%, with an average of 2.46%, and the contents of CaO and MgO are 0.46–1.86% and 0.39–0.76%, with an average of 1.17% and 0.55%, respectively. The TiO2 content is low, ranging from 0.15% to 0.42%, with an average value of 0.27%.
The loss on ignition (LOI) of most Dongping granite samples is less than 2% (Figure 3a). The sample points fall into the granite category in the SiO2- (Na2O + K2O) diagram (Figure 3b) and in the high-potassium calc–alkali–potassium basalt category in the SiO2-K2O diagram (Figure 3c). The aluminum saturation index (A/CNK) ranges from 0.95 to 1.80, indicating that the rocks are weakly to strongly peraluminous (Figure 3d).

4.2. Trace Elements and Rare-Earth Elements

The trace element contents in the Dongping granite samples vary greatly, and Ba, Sr, and Zr have the highest concentrations (Table 2). The Ba content ranges from 529.94 to 2472.90 ug/g, with an average value of 1085.95 ug/g. The Sr content ranges from 149.60 to 474.47 ug/g, with an average value of 277.79 ug/g, and the Zr content ranges from 133.063 to 315.19 ug/g, with an average value of 210.15 ug/g. The contents of U, Th, and Hf are 0.89–6.89 ug/g, 10.47–30.13 ug/g, and 3.70–8.12 ug/g, respectively, with averages of 3.33 ug/g, 17.67 ug/g, and 2.60 ug/g, respectively. The ∑REE values of the Dongping granite samples range from 90.66 ug/g to 246.96 ug/g, with an average value of 153.35 ug/g, and the LREE/heavy REE (HREE) values range from 10.60 to 34.17, with an average value of 20.70. The (La/Yb)N values range from 11.51 to 68.41 with an average value of 31.00, and the δEu values range from 0.49 to 1.11 with an average value of 0.67.
The trace element characteristics of the core samples from the three wells are similar in the primitive mantle-normalized trace element spider diagram (Figure 4a). The high Rb and low Sr contents reflect the dominance of K-feldspar and plagioclase feldspar in the crystallization of granite [38]. The REE patterns (Figure 4b) of all samples show consistent trends, with high LREE enrichment, strong HREE depletion, and a slightly negative Eu anomaly [39]. They are more similar to adakitic rocks and generally do not fall within the range of typical island-arc volcanic rocks. The results indicate that the samples may have originated from the partial melting of the crust, and the tectonic background of their formation may have been the extensional period after oceanic crust closure collisional orogeny.

5. Discussion

5.1. Granite Type

Based on the similar patterns in the REE diagram and trace element spider diagram (Figure 4), it can be inferred that the samples from different wells are products of the same magmatic–tectonic period and are derived from the same source.
Granites can be classified genetically into A, I, and S types [40,41]. A-type granites are deep-sourced rocks generally believed to have formed in extensional or non-compressional tectonic environments. Magmatism associated with A-type granites includes non-orogenic rift, intraplate, and post-orogenic magmatism following crustal thickening [13]. The TFe2O3/MgO ratio of the Early Paleozoic Dongping granites ranges from 4.41 to 4.58, with an average of 4.50, which is significantly higher than that of global typical I-type granites (with an average value of 2.27) and S-type granites (with an average value of 2.38). These granites plot in the A-type granite range in the (TFe2O3/MgO)-SiO2 and K2O-Na2O granite discrimination diagrams (Figure 5a,b). Furthermore, the REE patterns show LREE enrichment with low to moderate negative Eu anomalies (δEu ranging from 0.49 to 1.11), exhibiting a rightward inclination, which is consistent with the characteristics of A-type granites identified in previous studies [13,17].
Based on the trace element composition, such as Sr and Y, the granites can be divided into high-Sr/Y adakitic rocks and low-Sr/Y non-adakitic rocks. Adakitic rocks are characterized by high SiO2 (>56%) and Al2O3 (>15%) contents, high Sr/Y (>20.0) and La/Yb (>15.0) values, low MgO (<3%) content, high LREE enrichment, strong HREE depletion, and a slightly negative Eu anomaly. The samples exhibit high silica (69.94–75.19%) and aluminum (12.45–15.63%) contents, LREE enrichment, HREE depletion (i.e., significant LREE/HREE fractionation (LREE/HREE = 10.60–34.17)), La/Yb values of 16.95–100.71 (greater than 15.0), slightly negative Eu anomalies, and Sr/Y ratios of 12.27–132.64 (mostly >20), exhibiting geochemical characteristics similar to adakitic rocks. In the Sr/Y-Y and (La/Yb)N-YbN diagrams (Figure 5c,d), the samples plot between adakitic rocks and typical island-arc volcanic rocks. They are more similar to adakitic rocks and generally do not fall within the range of typical island-arc volcanic rocks. The results indicate that the samples may have originated from the partial melting of the crust, and the tectonic background of their formation may have been the extensional period after oceanic crust closure collisional orogeny.

5.2. Source Characteristics

Current research suggests that granite was formed primarily by the partial melting of the crust, crust–mantle magma mixing, and fractional crystallization of mantle-derived basic magmas [38]. Typically, the melting of clastic sedimentary rocks in the crust forms acidic peraluminous granites, whereas the melting of basic rocks forms metaluminous granites with more basic compositions [20,39]. Most Early Paleozoic granites from the SAOB plot within the range of basic rocks and graywacke components, suggesting a source region dominated by basic rocks (Figure 6a,b). Additionally, the geochemical characteristics of the rocks are similar to the upper crustal composition (Figure 6c,d). The rocks plot near the upper crustal composition in the Ta/Yb-Th/Yb diagram, indicating that they primarily originated from a mixed source of recycled and juvenile crustal material.
The solid/melt partition coefficients of incompatible trace elements can be used to distinguish fractional crystallization and partial melting. The partial melting trajectories are oblique lines, whereas the fractional crystallization trajectories are horizontal lines. The Early Paleozoic granites display oblique line trajectories (Figure 6d), indicating that the granites formed by magmatic activity experienced partial melting.

5.3. Tectonic Setting

The northern Tibetan Plateau is an Early Paleozoic orogenic system formed by the closure of the Proto-Tethys Ocean and is divided by the AOB. Previous researchers have conducted extensive U-Pb dating studies on the granite in the research area, with the formation time mostly between 407 and 420 Ma. Its material composition and tectonic framework record the evolution of the Proto-Tethys Ocean [49]. The SAOB, a continental subduction–collision orogenic belt, experienced an ocean–continent transition during the Early Paleozoic [19], with a paleogeographic landscape of ocean basins, micro-continents, multiple continents, and multi-island oceans [50,51]. The development of numerous multi-period Early Paleozoic granitic rocks in this region is of great significance for reconstructing the Early Paleozoic tectonic evolution of the South Altun region [4].
Kang et al. (2016) conducted systematic research on the timing, source characteristics, and formation mechanisms of magmatism at different stages of the SAOB [17]. They proposed that the region was characterized by oceanic ridge expansion and plate subduction in the “South Altun Ocean Basin” before 500 Ma, composed of E-MORB and N-MORB type basic–ultrabasic magmatic rocks and O-type adakites, which intruded as dykes or small stocks into the South Altun ophiolitic mélange with limited distribution. From 497 to 472 Ma, I-type and S-type granites with C-type adakitic characteristics formed, representing products of the high-pressure partial melting of upper crustal sandy rocks and lower crustal basaltic rocks during the continental crust’s deep subduction stage of collisional orogeny. This period represents an episode of crustal melting and granitic magma intrusion in the Late Cambrian of the Early Paleozoic South Altun [30,52]. From 469 to 445 Ma, OIB-type alkaline basic–ultrabasic rocks and I-type to S-type granites intruded into the South Altun metamorphic terrane as batholiths or stocks, showing characteristics of syn-exhumation magmatism after slab break-off. The former formed in an intracontinental extensional rifting environment, whereas the latter is characterized by low Sr (or high Sr) and high Y concentrations and a low Sr/Y ratio (with some high Sr and low Y contents), representing products of upper crustal exhumation-related decompression partial melting (locally still under compression). This stage was the initial post-collisional extensional crustal exhumation phase, reflecting the most intense regional tectonic–magmatic–thermal event of crust-derived granitic and mantle-derived basic magma intrusion in the Early Paleozoic South Altun [8,23,53]. From 424 to 385 Ma, as the continent–continent collision neared its end, the post-collisional extensional stage was characterized by A-type magmatic rocks with low Sr and high Y contents, exposed as stocks or dykes within the main fault zone of the southern Altun margin. These components are products of the high-temperature, low-pressure partial melting of the upper crust, representing the latest magmatic event of the Paleozoic granite in the southern Altun margin [7,54].
All granite samples from the Dongping area fall within the post-collisional granite, volcanic arc granite, and syn-collisional granite regions in the Rb- (Y + Nb) diagram (Figure 7a). Similarly, they plot within the collision granite, volcanic arc granite, and syn-collisional granite areas in the Nb-Y, Ta-Yb, and Rb- (Yb + Ta) diagrams (Figure 7b–d), with a predominance of post-collisional granites. This finding suggests that the Early Paleozoic granites in the SAOB likely formed in post-collisional extensional environments and syn-collisional volcanic arc tectonic settings.
Most samples plot in the post-orogenic granite region in the Al2O3-SiO2 and R1-R2 diagrams (Figure 8), with a few in the syn-collisional granite region. The granites in this study are dated at ~418 Ma [32]. Thus, it can be inferred that their tectonic environment was likely a transitional environment from continental subduction–collision orogeny to post-collisional extension (Figure 8). This period marks the beginning of continuous crustal extension and thinning, which may be related to the closure of multiple Proto-Tethys branch oceans in the northern Tibetan Plateau during the Early Paleozoic, leading to the amalgamation of multiple continental blocks and widespread collisional orogenesis [55].
Applsci 15 12239 g007
Figure 7. Tectonic environment discrimination diagrams for the Dongping granite (modified from [20,56]). (a) Rb vs. (Y + Nb), (b) NB vs. Y, (c) Ta vs. Tb, (d) Rb vs. Yb + Ta. Diagrams (a,b) are modified after [46], while (c) and (d) are modified after [47,48].
Figure 7. Tectonic environment discrimination diagrams for the Dongping granite (modified from [20,56]). (a) Rb vs. (Y + Nb), (b) NB vs. Y, (c) Ta vs. Tb, (d) Rb vs. Yb + Ta. Diagrams (a,b) are modified after [46], while (c) and (d) are modified after [47,48].
Applsci 15 12239 g007
Applsci 15 12239 g008
Figure 8. Tectonic discrimination diagram for the Dongping granite: (a) Al2O3 vs. SiO2 (modified from [38]), (b) R2 vs. R1 (modified from [57]). R1 = 4 × Si − 11 × (Na + K)-2 × (Fe + Ti), R2 = 6 × Ca + 2 × Mg + Al.
Figure 8. Tectonic discrimination diagram for the Dongping granite: (a) Al2O3 vs. SiO2 (modified from [38]), (b) R2 vs. R1 (modified from [57]). R1 = 4 × Si − 11 × (Na + K)-2 × (Fe + Ti), R2 = 6 × Ca + 2 × Mg + Al.
Applsci 15 12239 g008

6. Conclusions

(1) The Early Paleozoic granites of the SAOB can be categorized into three types: granitic gneiss, altered granite, and monzogranite. The granites in the study area are metaluminous and have high alkali contents (avg. 7.63%) and high TFe2O3/MgO ratios (avg. 4.50). They can be classified as peraluminous calc–alkaline rocks. They are relatively enriched in Rb, Ba, Th, and U and depleted in Sr, Ta, Nb, and Sm. The REE patterns exhibit a rightward inclination, with significant fractionation between light and heavy REEs, and they have slightly negative Eu anomalies.
(2) The (TFe2O3/MgO)-SiO2 and K2O-Na2O granite discrimination diagrams indicate that the Early Paleozoic granites in the SOB are A-type granites. Their composition is similar to that of the upper crust, indicating they primarily originated from a mixed source of recycled and juvenile crustal material. The granites formed by magmatic activity underwent partial melting.
(3) According to the regional tectonic evolution history, the Early Paleozoic granites in the South Altun Orogenic Belt are closely related to the subduction and collision of the Qaidam Block toward the Central Altun Block. Most granites formed in an extensional thinning tectonic environment following collisional orogeny, whereas a small portion formed in a volcanic arc tectonic environment during the syn-collisional stage. This period marks the beginning of continuous crustal extension and thinning.

Author Contributions

Conceptualization, X.Z.; Methodology, X.Z. and S.F.; Formal analysis, Z.W.; Resources, B.W.; Data curation, B.W. and Z.F.; Writing—original draft, X.Z.; Writing—review & editing, S.F. and H.C.; Supervision, G.W.; Project administration, G.W. All authors have read and agreed to the published version of the manuscript.

Funding

This research received no external funding.

Institutional Review Board Statement

Not applicable.

Informed Consent Statement

Not applicable.

Data Availability Statement

The data presented in this study are openly available in https://zenodo.org/records/17050722 (accessed on 14 November 2025).

Conflicts of Interest

Authors Bo Wang, Zhixiong Wu and Haidong Cui were employed by the company Qinghai Oil Field Branch Company, China National Petroleum Corporation. 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.

Abbreviations

The following abbreviations are used in this manuscript:
AOB The Altun Orogenic Belt
DPAThe Dongping area
SAOBThe South Altun Orogenic Belt
SAOMB The Southern Altun Ophiolitic Mélange Belt

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Applsci 15 12239 g001
Figure 1. Schematic geological map of the Altun region. Modified after [22]. (a) Geographical location map of Qaidam Basin. (b) Schematic diagram of the geological structure of the Qaidam Basin. (c) Geological map and sample distribution of the research area.
Figure 1. Schematic geological map of the Altun region. Modified after [22]. (a) Geographical location map of Qaidam Basin. (b) Schematic diagram of the geological structure of the Qaidam Basin. (c) Geological map and sample distribution of the research area.
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Applsci 15 12239 g002
Figure 2. Microscopic characteristics of leptite and granite in the study area. Qtz—quartz, Pl—plagioclase, Kfs—K-feldspar, Bt—biotite, Chl—chlorite, Ser—sericite.
Figure 2. Microscopic characteristics of leptite and granite in the study area. Qtz—quartz, Pl—plagioclase, Kfs—K-feldspar, Bt—biotite, Chl—chlorite, Ser—sericite.
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Figure 3. Geochemical diagrams of the Dongping granite: (a) loss on ignition (LOI) vs. SiO2 (Modified from [34]), (b) total alkalis (Na2O + K2O) vs. SiO2 (modified from [35]), (c) K2O vs. SiO2 (modified from [36]), and (d) A/CNK vs. A/NK (modified from [37]). A/CN and A/CNK represent the molar ratios of Al2O3 to (CaO + Na2O) and Al2O3 to (CaO + Na2O + K2O), respectively.
Figure 3. Geochemical diagrams of the Dongping granite: (a) loss on ignition (LOI) vs. SiO2 (Modified from [34]), (b) total alkalis (Na2O + K2O) vs. SiO2 (modified from [35]), (c) K2O vs. SiO2 (modified from [36]), and (d) A/CNK vs. A/NK (modified from [37]). A/CN and A/CNK represent the molar ratios of Al2O3 to (CaO + Na2O) and Al2O3 to (CaO + Na2O + K2O), respectively.
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Figure 4. (a) Primitive mantle-normalized trace element spider diagram and (b) chondrite-normalized rare-earth element (REE) pattern for the Dongping granite. The normalization values of primitive values are from [39].
Figure 4. (a) Primitive mantle-normalized trace element spider diagram and (b) chondrite-normalized rare-earth element (REE) pattern for the Dongping granite. The normalization values of primitive values are from [39].
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Figure 5. Discrimination diagrams for the Dongping granite type. (a) TFe2O3/MgO vs. SiO2 (modified from [42]), (b) Na2O vs. K2O (modified from [43]), (c) Sr/Y vs. Y, and (d) Ybₙ vs. (La/Yb)ₙ (modified from [44,45]).
Figure 5. Discrimination diagrams for the Dongping granite type. (a) TFe2O3/MgO vs. SiO2 (modified from [42]), (b) Na2O vs. K2O (modified from [43]), (c) Sr/Y vs. Y, and (d) Ybₙ vs. (La/Yb)ₙ (modified from [44,45]).
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Figure 6. Source discrimination diagrams for the Dongping granite. (a) (Na2O + K2O)/(TFe2O3 + MgO + TiO2) vs. (Na2O + K2O + TFe2O3 + MgO + TiO2), (b) Al2O3/ (TFe2O3 + MgO + TiO2) vs. (Al2O3 + TFe2O3 + MgO + TiO2), (c) Th/Yb vs. Ta/Yb, (d) La/Sm vs. La. Diagrams (a,b) are modified after [46], while (c,d) are modified after [47,48], respectively.
Figure 6. Source discrimination diagrams for the Dongping granite. (a) (Na2O + K2O)/(TFe2O3 + MgO + TiO2) vs. (Na2O + K2O + TFe2O3 + MgO + TiO2), (b) Al2O3/ (TFe2O3 + MgO + TiO2) vs. (Al2O3 + TFe2O3 + MgO + TiO2), (c) Th/Yb vs. Ta/Yb, (d) La/Sm vs. La. Diagrams (a,b) are modified after [46], while (c,d) are modified after [47,48], respectively.
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Table 1. Main elements of Dongping granite. Partial data quoted from Liu Jun et al., 2023 [32].
Table 1. Main elements of Dongping granite. Partial data quoted from Liu Jun et al., 2023 [32].
WellDP306DP5DP7DPH301-1DP1H-2-3
Sample NumberDP306-1DP306-2DP306-3DP5-1DP5-2DP5-3DP7-1DP7-2DPH301-1DPH301-2DP1H-2-3-1DP1H-2-3-2DP1H-2-3-3DP1H-2-3-4DP1H-2-3-5
Depth (m)1917.391913.321908.752653.462652.812652.5621712169.241878.961892.55
LithologyMigmatiteMonzograniteLeptiteGranitic GneissGranitic GneissGranitic GneissGranodioriteLeptiteGranitic GneissGranitic GneissGranitic GneissGranitic GneissGranitic GneissGranitic GneissGranitic Gneiss
SiO2 (%)73.0974.1774.2970.7169.9571.7774.6171.3973.7875.271.9270.1270.4470.3172.54
TiO2 (%)0.20.170.190.250.250.270.310.190.150.160.390.350.410.420.35
Al2O3 (%)13.9713.613.5314.0914.3913.914.0914.8313.7512.4614.9315.6414.714.8214.08
TFe2O3 (%)2.231.881.832.472.722.422.132.431.722.012.962.943.482.932.76
MnO (%)0.060.050.050.080.090.070.040.060.050.060.040.050.080.070.06
MgO (%)0.480.390.450.560.630.50.540.430.420.420.580.670.760.750.63
CaO (%)1.190.811.551.811.861.280.571.291.551.380.580.461.321.210.75
Na2O (%)3.33.333.254.553.254.390.812.733.273.193.1833.032.882.46
K2O (%)4.284.474.173.814.884.355.015.64.63.483.985.374.134.574.19
P2O5 (%)0.050.040.050.070.070.080.070.060.040.040.110.110.120.120.12
LOI (%)0.560.450.971.832.261.431.670.991.070.921.371.311.591.811.62
TOTAL (%)99.4199.35100.32100.22100.35100.4499.86100100.3999.31100.05100.02100.0799.999.55
Table 2. Trace elements and rare-earth elements of Dongping granite.
Table 2. Trace elements and rare-earth elements of Dongping granite.
WellSample NumberDepth
(m)		7Li
(ug/g)		9Be
(ug/g)		45Sc
(ug/g)		51V
(ug/g)		52Cr
(ug/g)		59Co
(ug/g)		60Ni
(ug/g)		65Cu
(ug/g)		66Zn
(ug/g)		71Ga
(ug/g)		74Ge
(ug/g)
DP7DP-7-242171.598.502.812.249.686.3462.754.403.3877.5517.680.67
DP7-252169.289.973.163.709.954.1768.381.561.0262.1520.150.96
DP1H-2-3DP1H-2-3-153187.5916.871.932.1914.065.1947.681.697.7846.8518.960.94
DP1H-2-3-133180.9813.961.812.4114.904.6949.882.448.8163.4318.521.02
DP1H-2-3-103088.525.911.211.468.024.7242.792.045.1930.3317.030.89
DP1H-2-3-73078.2911.571.623.4719.074.6824.792.415.9044.3717.360.87
DP306DP306-6-31908.7544.632.932.267.914.9972.283.006.3264.6517.481.19
DP306-6-11917.3947.082.381.2811.013.5241.751.361.6952.4317.120.95
DP306-6-21913.3253.552.961.637.853.4564.111.211.1442.4017.961.14
Average Value
(ug/g)		 42.452.312.2911.384.6452.712.234.5853.7918.030.96
Maximum
(ug/g)		 5.911.211.287.853.4524.791.211.0230.3317.030.67
Minimum
(ug/g)		 98.503.163.7019.076.3472.284.408.8177.5520.151.19
WellSample NumberDepth
(m)		80Ar2
(ug/g)		85Rb
(ug/g)		88Sr
(ug/g)		89Y
(ug/g)		90Zr
(ug/g)		93Nb
(ug/g)		98Mo
(ug/g)		111Cd
(ug/g)		114Cd
(ug/g)		118Sn
(ug/g)		133Cs
(ug/g)
DP7DP-7-242171.52.37190.00166.9312.21211.8413.031.480.040.106.9134.94
DP7-252169.23.84180.81314.3016.31211.7416.241.150.040.128.2033.91
DP1H-2-3DP1H-2-3-153187.592.95124.97348.176.15315.1914.001.260.050.031.612.84
DP1H-2-3-133180.981.69129.59394.136.38305.4912.911.410.050.031.643.03
DP1H-2-3-103088.523.26187.69261.821.97143.248.381.430.020.021.263.11
DP1H-2-3-73078.293.8169.39474.4710.61268.1813.861.140.050.031.732.76
DP306DP306-6-31908.753.59151.66188.1714.06133.0614.181.570.040.127.228.84
DP306-6-11917.391.51197.23149.6012.20151.3213.411.010.040.106.419.55
DP306-6-21913.322.18186.70202.5011.30151.2711.031.240.030.096.139.56
Average Value
(ug/g)		 2.80157.56277.7910.13210.1513.001.300.040.074.5712.06
Maximum
(ug/g)		 1.5169.39149.601.97133.068.381.010.020.021.262.76
Minimum
(ug/g)		 3.84197.23474.4716.31315.1916.241.570.050.128.2034.94
WellSample NumberDepth
(m)		135Ba
(ug/g)		178Hf
(ug/g)		181Ta
(ug/g)		182W
(ug/g)		205Tl
(ug/g)		208Pb
(ug/g)		209Bi
(ug/g)		232Th
(ug/g)		238U
(ug/g)		139La
(ug/g)		140Ce
(ug/g)
DP7DP-7-242171.5646.785.640.83481.921.3425.000.1419.535.3539.1267.13
DP7-252169.2651.095.851.74509.791.3328.960.1630.136.8962.08112.92
DP1H-2-3DP1H-2-3-153187.591349.368.120.60400.410.7417.150.1015.022.8659.9676.14
DP1H-2-3-133180.981497.147.960.47384.810.6821.120.1216.692.8066.0579.34
DP1H-2-3-103088.522472.903.700.68349.091.0522.660.1310.470.8623.6544.78
DP1H-2-3-73078.291490.036.840.82196.960.6014.010.0818.412.4333.0583.24
DP306DP306-6-31908.75577.913.841.05608.701.2947.870.2717.572.7226.2870.33
DP306-6-11917.39529.944.170.52329.541.1832.850.1914.743.8322.9338.23
DP306-6-21913.32558.434.270.40478.031.1231.010.1716.472.2622.9540.52
Average Value
(ug/g)		 1085.955.600.79415.471.0426.740.1517.673.3339.5668.07
Maximum
(ug/g)		 529.943.700.40196.960.6014.010.0810.470.8622.9338.23
Minimum
(ug/g)		 2472.908.121.74608.701.3447.870.2730.136.8966.05112.92
WellSample NumberDepth
(m)		141Pr
(ug/g)		146Nd
(ug/g)		149Sm
(ug/g)		151Eu
(ug/g)		160Gd
(ug/g)		159Tb
(ug/g)		164Dy
(ug/g)		165Ho
(ug/g)		166Er
(ug/g)		172Yb
(ug/g)		175Lu
(ug/g)
DP7DP-7-242171.57.6726.683.970.683.140.352.440.451.091.250.19
DP7-252169.212.0640.365.801.074.460.563.400.621.501.690.25
DP1H-2-3DP1H-2-3-153187.5910.7334.984.190.822.680.201.540.270.630.660.10
DP1H-2-3-133180.9811.2235.444.200.922.700.231.610.280.650.660.10
DP1H-2-3-103088.525.1817.542.110.641.240.000.690.120.290.350.05
DP1H-2-3-73078.298.5029.984.430.903.220.322.160.390.941.050.16
DP306DP306-6-31908.755.5718.753.000.482.710.342.680.531.321.500.22
DP306-6-11917.394.4214.502.290.362.130.242.260.461.161.350.20
DP306-6-21913.324.4814.642.330.432.090.232.180.431.111.350.20
Average Value
(ug/g)		 7.7625.873.590.702.710.312.110.390.971.090.16
Maximum
(ug/g)		 4.4214.502.110.361.240.200.690.120.290.350.05
Minimum
(ug/g)		 12.0640.365.801.074.460.563.400.621.501.690.25
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MDPI and ACS Style

Zeng, X.; Fu, S.; Wang, G.; Wang, B.; Wu, Z.; Cui, H.; Feng, Z. The Geochemical Characteristics, Genesis, and Geological Significance of Early Paleozoic Granites in the South Altun Orogenic Belt of Western China. Appl. Sci. 2025, 15, 12239. https://doi.org/10.3390/app152212239

AMA Style

Zeng X, Fu S, Wang G, Wang B, Wu Z, Cui H, Feng Z. The Geochemical Characteristics, Genesis, and Geological Significance of Early Paleozoic Granites in the South Altun Orogenic Belt of Western China. Applied Sciences. 2025; 15(22):12239. https://doi.org/10.3390/app152212239

Chicago/Turabian Style

Zeng, Xu, Suotang Fu, Guiwen Wang, Bo Wang, Zhixiong Wu, Haidong Cui, and Zongqi Feng. 2025. "The Geochemical Characteristics, Genesis, and Geological Significance of Early Paleozoic Granites in the South Altun Orogenic Belt of Western China" Applied Sciences 15, no. 22: 12239. https://doi.org/10.3390/app152212239

APA Style

Zeng, X., Fu, S., Wang, G., Wang, B., Wu, Z., Cui, H., & Feng, Z. (2025). The Geochemical Characteristics, Genesis, and Geological Significance of Early Paleozoic Granites in the South Altun Orogenic Belt of Western China. Applied Sciences, 15(22), 12239. https://doi.org/10.3390/app152212239

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