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Article

Geochemical Characteristics of Sandstone-Type Uranium Deposits and Their Significance for Uranium Mineralization in Daqing Placanticline, Northern Songliao Basin

by
Chao Tang
1,2,*,
Lulu Chen
1,2,
Zenglian Xu
1,2,
Huajian Liu
1,2,
Jialin Wei
1,2 and
Peng Xiao
1,2
1
Tianjin Centre, China Geological Survey, Tianjin 300170, China
2
Laboratory of Non-Fossil Energy Minerals, Tianjin Center of China Geological Survey, Tianjin 300170, China
*
Author to whom correspondence should be addressed.
Minerals 2026, 16(9), 953; https://doi.org/10.3390/min16090953 (registering DOI)
Submission received: 18 August 2026 / Revised: 12 September 2026 / Accepted: 13 September 2026 / Published: 18 September 2026
(This article belongs to the Special Issue Critical Metal Minerals, 2nd Edition)
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Abstract

To reveal the uranium enrichment mechanism in the Daqing Placanticline area, northern Songliao Basin, this study collected a total of 41 samples of three geological types, namely uranium ore, uranium-mineralized sandstone and host rock from the Upper Cretaceous Sifangtai Formation. Combined with 109 geochemical datasets from exploration, systematic analyses were performed on major elements, trace elements, rare earth elements (REE), total organic carbon (TOC), total sulfur and other key geochemical parameters. The results indicate that uranium ore and mineralized sandstone are generally characterized by high TOC, high total sulfur, low Th/U and low Fe2O3/FeO ratios, while host rocks show the opposite geochemical assemblage, suggesting uranium enrichment took place in a strongly reducing sedimentary environment. The ore-forming system is significantly enriched in trace elements including U, Pb, Mo, Ba, Zn and Y, and depleted in Cu, Co, Ni, Cr, Sr, Nb, Ta, Zr and Hf. Among these elements, Mo and Pb have an extremely close relationship with uranium mineralization and can be used as effective ore-forming indicator elements. Uranium ore, mineralized sandstone and host rock exhibit consistent REE distribution patterns, implying that the strata in the study area share uniform provenance, sedimentary environment and tectonic setting. Some high-grade uranium ores are obviously enriched in heavy rare earth elements (HREE), demonstrating fluid modification during the late mineralization stage. Combined with regional tectonic evolution and hydrocarbon migration features, this study concludes that sandstone-type uranium deposits in the Daqing Placanticline mainly underwent two stages of mineralization: supergene fluid mineralization and superimposed reworking by deep hydrocarbon-bearing reducing fluids.

1. Introduction

Uranium, as a critical strategic energy resource, is of great significance to social production and economic development [1,2]. Numerous types of uranium deposits with industrial significance occur worldwide, including unconformity-related, sandstone-type, breccia-hosted, granite-related and volcanic-hosted deposits. Owing to advantages such as low mining cost and environmental friendliness, sandstone-type uranium deposits have become the most important type exploited globally [3,4,5]. Statistics show that sandstone-type uranium deposits account for approximately 30% of the global uranium resources and more than 50% of global uranium production [6,7,8]. Uranium exploration and exploitation in China are also largely focused on sandstone-type uranium deposits [2,5]. Most sandstone-type uranium deposits occur in Meso-Cenozoic sedimentary basins between 25° N and 50° N in the Northern Hemisphere and were mostly formed in the Late Mesozoic to Cenozoic [3,9,10,11]. Large-scale anomalous enrichment of sandstone-type uranium also occurs in the Meso-Cenozoic sedimentary basins in northern China, where a series of sandstone-type uranium deposits have been discovered successively in the Yili Basin, Turpan-Hami Basin, Ordos Basin, Erlian Basin, Songliao Basin and other basins [12,13,14]. The Songliao Basin is located in the eastern extension of the giant Central Asian sandstone-type uranium metallogenic belt, and uranium deposits are mainly distributed in Qianjiadian, Baixingtu and other areas on the southwestern margin of the basin [15,16]. In recent years, industrial uranium orebodies have been discovered in the Upper Cretaceous Sifangtai Formation in the Daqing Placanticline area of the northern Songliao Basin, demonstrating excellent prospecting potential [17] and attracting widespread attention from researchers. Relevant studies have mainly focused on the stratigraphic sequence architecture and sedimentary environment of the Sifangtai Formation [18], provenance analysis [19,20], occurrence states of uranium minerals [21,22], and fine inversion prediction of seismic data [23,24]. However, research on the geochemical characteristics of uranium deposits in this area remains relatively inadequate.
Sandstone-type uranium deposits are typical products of supergene mineralization driven by basin–mountain coupling. Uranium enrichment and mineralization occur when uranium-bearing ore-forming fluids interact at redox interfaces via redox reactions and adsorption [25,26]. During mineralization, oxygenated uranium-bearing fluids undergo water–rock reactions with host rocks, triggering dissolution, replacement, recrystallization of primary minerals and authigenic cementation. These processes inevitably lead to element migration (element import and export). For this reason, geochemical characteristics of uranium ores and host rocks are widely used to reconstruct ore-forming processes and summarize exploration indicators [27,28,29,30]. In recent years, some researchers have also utilized uranium-rich mineral-bearing sandstones to constrain the origin and formation age of sandstone units [31]. Taking the Upper Cretaceous Sifangtai Formation and its uranium mineralization in the Daqing Placanticline as the research objects, this paper, on the basis of summarizing the geological characteristics of uranium mineralization, conducts an elemental geochemical study on three types of geological bodies, namely sandstone-type uranium ore (w(U) ≥ 100 × 10−6), uranium-mineralized sandstone (w(U) 20~100 × 10−6) and wall rock (w(U) ≤ 20 × 10−6). This study aims to obtain a systematic understanding of the metallogenic geochemical characteristics of sandstone-type uranium deposits in the basin and attempts to discuss the uranium mineralization process.

2. Geological Setting

The Songliao Basin, located in the northeastern part of China, is a large Meso-Cenozoic fault-depression to depression-type continental petroliferous basin with polycyclic characteristics, hosting abundant oil and gas resources and sedimentary minerals [32,33]. Its formation and evolution are under a complex geological setting: the basin is not only a product of continental crustal rifting but also a result of the long-term extensional tectonism of the continental crust, occasionally accompanied by compressional tectonic activities [34,35,36,37]. The basin is surrounded by mountain ranges including the Greater Khingan Mountains, Lesser Khingan Mountains and Zhangguangcai Mountains, stretching in a north-northeast direction with a length of approximately 750 km, a width of 330~370 km and a total area of about 260,000 square kilometers [38] (Figure 1a,b). The basin is formed by the amalgamation of multiple blocks including the Erguna Block, Xing’an Block, Songnen Block, and Bureya-Jiamusi-Xingkai Block, with its main body situated on the Songnen Block. Based on the basement properties, fault characteristics and regional stratigraphic distribution, the Songliao Basin is divided into six first-order tectonic units, namely the Western Slope Zone, Central Depression Zone, Northern Plunge Zone, Northeastern Uplift Zone, Southeastern Uplift Zone and Southwestern Uplift Zone [39] (Figure 1b). The Central Depression Zone is located in the central part of the basin and is a large-scale negative tectonic unit with relatively dominant subsidence during the basin’s evolutionary process. It has long served as the subsidence and sedimentary center of the basin, where the sedimentary cover is complete and multiple sets of petroleum source–reservoir–cap assemblages are developed. As the most important oil and gas source area and the concentrated distribution area of oil and gas fields in the basin, the study area of this paper is situated at the southern tip of the Daqing Placanticline Uplift, a second-order positive tectonic unit within the Central Depression Zone (Figure 1c).
The basement of the Songliao Basin is mainly composed of medium-deep metamorphic rocks, low-grade metamorphic rocks and granites [42,43,44,45,46]. The medium-deep metamorphic rock series are predominantly distributed in a zonal pattern along the major axis of the basin, with lithologies mainly including gneiss, granitic gneiss, schist and metamorphic sandstone. The low-grade metamorphic rock series are distributed on both sides of the medium-deep metamorphic rock series, dominated by slate and metamorphic sandstone. Granite intrusions are mainly distributed in the northern part of the basin. All the above basement rock types are exposed at the basin margins, which largely control the composition and distribution of Mesozoic sedimentary rocks within the basin. The sedimentary cover of the basin is filled with clastic deposits of Late Mesozoic to Cenozoic age with a thickness of approximately 10 km [47,48], which are mainly composed of the Jurassic, Cretaceous, Paleogene, Neogene and Quaternary systems. These are subdivided in sequence into the Upper Jurassic Huoshiling Formation; the Lower Cretaceous Shahezi, Yingcheng, Denglouku and Quantou Formations; the Upper Cretaceous Qingshankou, Yaojia, Nenjiang, Sifangtai and Mingshui Formations; the Tertiary Yi’an, Da’an and Taikang Formations; and the Quaternary system. Among these, the Cretaceous strata are the most completely developed and thickest. The Quantou and Nenjiang Formations represent important hydrocarbon reservoirs within the basin and have experienced multiple episodes of hydrocarbon charging. Large-scale hydrocarbon expulsion occurred particularly at the end of the Mingshui Formation, whereby deep hydrocarbons migrated upward along faults into the overlying Sifangtai Formation. Granites and volcanic rocks of the Caledonian, Hercynian and Yanshanian periods are widely distributed around the Songliao Basin, and their weathering and denudation can provide an abundant provenance and uranium source for uranium mineralization in the basin [49]. The latest uplift event during the Oligocene-Miocene epoch has exerted a significant influence on the formation of sandstone-type uranium deposits [50,51].

3. Mining Area Geology

3.1. Stratigraphic Architecture of the Cretaceous System

Drilling reveals that the Cretaceous strata in the study area consist of the Nenjiang Formation, Sifangtai Formation and Mingshui Formation from bottom to top. The Nenjiang Formation (K2n) represents a set of shallow lacustrine sedimentary formations, with a lithologic association of light-gray and dark-gray mudstones intercalated with reddish-brown silty mudstones. It has poor water permeability and serves as an important aquiclude for the uranium-bearing horizons of the Sifangtai Formation. The Sifangtai Formation (K2s) is the main uranium-bearing horizon in the study area, with a stratigraphic thickness of 60~200 m. It constitutes a set of variegated fine-clastic rock intercalated with mudstone sedimentary formations formed in fluvial and fluvio-lacustrine delta facies, and its lithology is dominated by thick-bedded light-gray and greenish-gray fine sandstones intercalated with reddish-brown mudstones and argillaceous siltstones. The formation has an unconformable contact with the underlying Nenjiang Formation. The Mingshui Formation (K2m) has a stratigraphic thickness of 90~120 m. Its lower part consists of a set of light-gray fluvial channel deposits, dominated by gray fine sandstones intercalated with thin layers of gray glutenite, while the upper part comprises a set of red sedimentary formations, mainly red mudstones and silty mudstones intercalated with thin layers of light-gray fine sandstones. The Sifangtai Formation (K2s) in the study area is well developed, complete and stable, which controls the overall distribution of sandstone-type uranium deposits and provides favorable reservoir conditions for uranium mineralization.

3.2. Lithological and Lithofacies Characteristics of the Sifangtai Formation

Based on variations in lithology and lithofacies as well as sedimentary characteristics, the Sifangtai Formation is divided into three lithologic members (Figure 2).
  • Lower Member of the Sifangtai Formation (K2s1): It represents a meandering river deposit formed in a humid climatic environment during the early sedimentary stage, with a thickness of 20~35 m. Its lithology is dominated by gray and grayish-green fine sandstone, medium-coarse sandstone and pebbly sandstone. It has an abrupt contact with the mudstone of the Nenjiang Formation at the base, with developed erosion surfaces and commonly observed trough and tabular cross-beddings. Carbonaceous laminae are widespread in the gray sandstones, while pyrite is rare. The sandstones locally contain abundant flat and subrounded mud gravels and gravels with unsorted sizes and oriented arrangement. The above characteristics indicate that the Lower Member of the Sifangtai Formation represents channel bottom lag deposits with well-developed sand bodies and abundant reducing media such as carbon fragments and organic matter. It has a close association with uranium mineralization and serves as the main uranium-bearing horizon in the study area.
  • Middle Member of the Sifangtai Formation (K2s2): It corresponds to shore-shallow lacustrine facies deposits, with flood plain deposits developed locally, and has a thickness of 35~55 m. Its lithology is dominated by light-grayish-green, light-gray, purplish-red and brownish-red argillaceous siltstones and silty mudstones, with thin-bedded sandstones intercalated in between. This member is dominated by fine-grained deposits with poor water permeability, serving as the upper aquiclude for the Lower Member of the Sifangtai Formation.
  • Upper Member of the Sifangtai Formation (K2s3): It corresponds to meandering river deposits formed under arid paleoclimatic conditions, with a thickness of 25~50 m. Its lower part is lithologically dominated by light-gray, light-grayish-green and brownish-red fine sandstones and siltstones, with grayish-white calcareous sandstone bands intercalated locally, and calcareous concretions, calcareous lumps and mud gravels are well developed. The upper part is dominated by fine-grained deposits such as brownish-red variegated argillaceous siltstones and silty mudstones intercalated with purplish-red, brown, light-gray and light-grayish-green facies, with thin layers of light-gray siltstones intercalated locally. The hydrodynamic force during the sedimentary stage of this member was stronger than that of the Middle Member of the Sifangtai Formation; sand bodies of a certain thickness are developed in some drill holes with good water permeability, which can also form favorable uranium reservoirs.
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Figure 2. Comprehensive stratigraphic Profile L1 of the Daqing Placanticline area in the Northern Songliao Basin. Section L1 is shown in Figure 1c.
Figure 2. Comprehensive stratigraphic Profile L1 of the Daqing Placanticline area in the Northern Songliao Basin. Section L1 is shown in Figure 1c.
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3.3. Permeability of the Sandstone Strata of the Sifangtai Formation

One of the key conditions for the formation of sandstone-type uranium deposits is that the sandstone strata must possess favorable permeability. A statistical analysis of the permeability coefficient (kφ) of ore samples from the study area shows the following results: the kφ of mudstone ranges from 0.01 to 0.21 m/d with an average of 0.11 m/d; the kφ of siltstone ranges from 0.21 to 0.49 m/d with an average of 0.35 m/d; the kφ of fine sandstone ranges from 0.18 to 10.16 m/d with an average of 2.45 m/d; the kφ of medium sandstone ranges from 0.20 to 8.77 m/d with an average of 3.59 m/d; and the kφ of coarse sandstone ranges from 0.95 to 4.08 m/d with an average of 2.52 m/d. Excluding mudstone, the kφ of sandstone samples in the study area varies from 0.18 to 10.16 m/d, with an average of 0.35 to 3.59 m/d. Overall, the strata are classified as weakly to moderately permeable, which is relatively favorable for the formation of sandstone-type uranium deposits.

3.4. Characteristics of Uranium Orebodies

Based on the statistics of mineralization from drilling surveys, three uranium mineralization layers are developed in the Sifangtai Formation. The mineralization layer in the Upper Member of the Sifangtai Formation is dominated by mudstone mineralization; the mineralization layer in the Middle Member is characterized by both sandstone and mudstone mineralization; and the mineralization layer in the Lower Member is dominated by sandstone mineralization, which constitutes the industrial ore layer. On the plane, uranium mineralization in the Sifangtai Formation has a wide distribution, forming three mineralization enrichment areas, namely Guqia, Toutai and Daxing (Figure 1c). The industrial uranium orebodies are generally tabular and lenticular in shape (Figure 2). The buried depth of the top interface of the orebodies ranges from 206 to 407 m, and that of the bottom interface ranges from 209 to 412 m. The uranium orebodies in the Daxing area have the greatest buried depth, while those in the Guqia and Toutai areas are relatively shallowly buried. The uranium mineralization enrichment centers are obviously controlled by river channels, and industrial uranium mineralization is mainly hosted in the bottom channel lag and point bar microfacies.

3.5. Characteristics of Uranium Ore

The main types of uranium ore in the Sifangtai Formation include medium sandstone-type, fine sandstone-type, siltstone-type and mudstone-type, with a small amount of coarse sandstone-type. Among them, industrial uranium ore is mostly fine sandstone-type and medium sandstone-type, characterized by loose texture and good water permeability. There are differences in the ore types among various mineralization enrichment areas: the ores in Daxing and Guqia are dominated by medium sandstone-type, while those in Toutai are mainly fine sandstone-type and siltstone-type. The main uranium minerals are pitchblende and coffinite. Uranium mineral grains are fine grained, mostly occurring as granular, spot-like, massive, banded, reticular, and zoned forms, as well as dispersed micrograins and microgranular aggregates, with grain sizes ranging from several μm to 200 μm. Uranium ores are mainly paragenetic with pyrite, quartz and feldspar, distributing between clastic grains or in fractures, filling in the cement of sandstones, or growing around pyrite to form a rim-like structure [23].

4. Samples and Analytical Methods

For this study, 11 representative drill holes of the sandstone-type uranium deposit in the Daqing Placanticline were selected, and 41 sandstone samples from the Lower Member of the Sifangtai Formation were collected (Table 1). During sample collection, an FD-3010A γ+β logging instrument was first used to measure gamma values. Host rocks, mineralized sandstones and uranium ores were classified according to the measured readings. For host rocks, we prioritized sampling unaltered sandstones. The determinations of whole-rock major, trace and rare earth elements were conducted at the Experimental Testing Center of Beijing Research Institute of Uranium Geology. First, the samples were crushed to 200 mesh without contamination. Whole-rock major elements were analyzed by an X-ray fluorescence spectrometer (AXIOS, Malvern Panalytical B.V., Almelo, The Netherlands) with a relative error of less than 5%. Trace elements and rare earth elements were determined by inductively coupled plasma mass spectrometry (ICP-MS, model Perkin Elmer Elan 6100 DRC, manufactured by PerkinElmer Inc., Waltham, MA, USA). During the test, standard reference materials AVG-1 and BHVO-1 were used for quality control of sample analysis, and the relative errors of the analytical results were generally less than 5%. The test results are presented in Table 2, Table 3 and Table 4. In addition, 109 geochemical index samples (e.g., total organic carbon, total sulfur) collected during the exploration work were collated, with the results shown in Table 5. These 109 samples were analyzed at the No.240 Research Institute of Nuclear Industry. The concentrations of uranium (U) and total sulfur were determined using inductively coupled plasma atomic emission spectrometry (ICP-AES, iCAP7200; Thermo Fisher Scientific, Waltham, MA, USA). The contents of Fe2+, Fe3+ and S2− were measured by ultraviolet–visible spectrophotometry. Total organic carbon was analyzed with a carbon–sulfur analyzer. pH values were tested using a combined glass electrode, and Eh values were measured by a platinum electrode paired with a reference electrode. The analytical precision for all tests was better than 5%. Both sets of samples were collected simultaneously during fieldwork, so their analytical data can be directly compared.

5. Results

Samples were statistically divided into three groups according to the geochemical properties of uranium and uranium ore grade: samples with w(U) ≤ 20 × 10−6 were defined as ore-free wall rocks, those with w(U) ranging from 20 × 10−6 to 100 × 10−6 as uranium-mineralized sandstones, and samples with w(U) ≥ 100 × 10−6 as uranium ores.

5.1. Geochemical Characteristics of Uranium, Thorium and Major Elements

Analytical results of major element oxides, uranium and thorium contents in the samples are presented in Table 2, from which the following characteristics can be observed (Figure 3): ① Th contents are similar in various sandstone types, indicating the relatively stable geochemical behavior of Th. However, the Th/U ratios vary significantly, with the ratios in wall rocks being much higher than those in uranium ores, which reflects the migration and leaching of U from the wall rocks. ② SiO2 is the most abundant component in the rocks, and uranium ores have the lowest SiO2 content (with an average of 70.56%), indicating the migration of Si during the uranium enrichment process. Al2O3 is the second most abundant component, and its content variation characteristics are consistent with those of K2O and Na2O, with no obvious changes in content observed across various sandstone types. ③ The contents of Fe2O3 and FeO and the Fe2O3/FeO ratios vary among different sandstone types: Fe2O3 has the highest content in wall rocks (with an average of 1.94%), while FeO is abundant in uranium ores (with an average of 0.90%). The Fe2O3/FeO ratios of wall rocks, uranium-mineralized sandstones and uranium ores are 3.51, 1.71 and 1.56, respectively, showing an inverse gradual change trend with U content, which reflects that uranium enrichment occurred in a relatively strong reducing environment. ④ CaO content is relatively high, with its mass fraction exceeding 1% in all sandstone types, and it increases significantly in uranium ores (with an average of 3.55%), which is 3.3 times the average content in wall rocks and uranium-mineralized sandstones. This indicates a strong carbonate alteration of sandstones in the study area. ⑤ MgO, TiO2, MnO and P2O5 contents are relatively low, with no obvious variations observed across all sandstone types.

5.2. Characteristics of Total Organic Carbon, Total Sulfur Contents, pH and Eh Values

Table 5 presents the statistical test results of 109 geochemical index samples of sandstones from the Lower Member of the Sifangtai Formation collected during the exploration work, from which the following can be observed: ① Total organic carbon (TOC) contents are relatively high in uranium ores and uranium-mineralized sandstones, with average values of 0.33× 10−6 and 0.22 × 10−6, respectively, and the lowest in wall rocks at an average of 0.16 × 10−6. Total sulfur (∑S) contents are the highest in uranium ores and the lowest in wall rocks. These characteristics indicate that the degree of uranium precipitation and enrichment is closely related to the contents of reducing substances (e.g., organic matter, pyrite) in the rocks, which is consistent with the field observation that ore-bearing bed rocks are mostly rich in carbonaceous laminae and pyrite. ② The pH values are highest in host rocks (average of 9.76), while uranium-mineralized sandstones and uranium ores show relatively lower values (averages of 9.55 and 9.56), showing a negative correlation with uranium content, which indicates that the uranium enrichment environment was a relatively weakly alkaline one. Eh values are the lowest in uranium ores and highest in uranium-mineralized sandstones, although the differences are small.

5.3. Characteristics of Trace Elements

Analytical results of trace element contents and characteristic parameters for the samples are presented in Table 3. Using the trace element contents of Chinese sedimentary rocks as the reference standard, spider diagrams of three sandstone types (wall rocks, uranium-mineralized sandstones and uranium ores) from the sandstone-type uranium deposit in the Daqing Placanticline were plotted (Figure 4), revealing the following characteristics: ① Uranium ore samples are significantly enriched in U, Pb, Mo, Ba, Zn and Y, among which U (103 × 10−6~4974 × 10−6) and Mo show intense enrichment with enrichment factors reaching as high as 2487 and 3543. Pb (14.1 × 10−6~357 × 10−6), Ba (395 × 10−6~898 × 10−6) and Zn (17 × 10−6~69 × 10−6) exhibit relatively strong enrichment; Y, as a rare earth element, shows relative enrichment in three samples. ② Uranium-mineralized sandstones are enriched in U, Pb, Mo and Ba, but the enrichment degree is lower than that of uranium ores; wall rocks are enriched in U, Pb and Ba, with the U content ranging from 1.91 × 10−6 to 9.27 × 10−6 and the enrichment factor varying from 0.96 to 4.64. This indicates that the sandstones in the study area have a relatively high overall U content, which can provide a part of the uranium source for uranium mineralization. ③ Wall rocks, uranium-mineralized sandstones and uranium ores all show a general depletion of Th, Cu, V, Co, Ni, Cr, Sr, Nb, Ta, Zr, Hf and other elements, and the variety of depleted elements tends to increase with the enhancement of U enrichment. ④ The spider diagrams of the three sandstone types (wall rocks, uranium-mineralized sandstones and uranium ores) are similar, differing only in the degrees of elemental enrichment and depletion. This indicates a common provenance signature, with subsequent modification by uranium-bearing fluids during the later stage.

5.4. Characteristics of Rare Earth Elements

Contents and characteristic ratios of rare earth elements in the samples (Table 4), and their chondrite-normalized distribution patterns (Figure 5), exhibit the following characteristics: ① The total rare earth element content (ΣREE) of the samples ranges from 74.51 to 229.44 × 10−6, with ΣLREE ranging from 66.86 to 208.16 × 10−6 and ΣHREE from 6.68 to 22.88 × 10−6. The LREE/HREE ratios vary from 6.19 to 12.93, with LREE contents significantly higher than HREE contents and high LREE/HREE ratios, indicating that the sandstones in the ore-bearing beds are enriched in LREE, depleted in HREE, and characterized by a high degree of LREE-HREE fractionation, which reflects a high maturity of crustal evolution in the source area. The chondrite-normalized (La/Sm)n ratios range from 3.46 to 5.04 and (Gd/Yb)n ratios range from 1.01 to 2.18, showing obvious fractionation of light rare earth elements and insignificant fractionation of heavy rare earth elements. The δEu values are between 0.55 and 0.91, indicating a moderate negative Eu anomaly, while the δCe values range from 0.91 to 1.01, with no obvious Ce anomaly. ② The rare earth element (REE) contents of the samples are significantly affected by lithology, with the REE contents in siltstone samples generally higher than those in other sandstone samples. In addition to lithological control, the REE contents in uranium ores show an increasing trend in total REE (ΣREE) and its individual fractions with the rise of uranium content, with a relatively large increase in heavy rare earth elements (HREE). This indicates that REE, especially HREE, were enriched during the uranium mineralization process. ③ The chondrite-normalized REE distribution patterns of the samples are basically identical, with the pattern showing a sloped trend before Eu and a flat trend after Eu as the boundary; the post-Eu segment of the pattern for uranium ore samples is obviously shifted upward.

6. Discussion

6.1. Correlation Analysis

In this study, nine charts illustrating the correlations between uranium (U) and other trace elements as well as rare earth elements were plotted (Figure 6) to investigate the extensive associations related to uranium enrichment. Figure 6a,b show the variation relationships between Th, Th/U ratio and uranium (U), respectively. It can be found that Th has a poor correlation with uranium (U) (R2 = 0.0727), while the Th/U ratio exhibits a significant negative correlation with uranium (U) (R2 = 0.9378). Figure 6c presents the correlation plot of molybdenum (Mo) against uranium (U), showing a distinct correlation between uranium and molybdenum contents (R2 = 0.6456). Figure 6d is the correlation plot of lead (Pb) against uranium (U), which exhibits a distinct linear correlation trend (R2 = 0.4019). Figure 6e,f show the variation relationships between Sc, Y and uranium (U), respectively. Figure 6g–i show the correlation plots of ΣREE, LREE and HREE against uranium (U), respectively. The correlation characteristics are similar to those of Sc and Y, with uranium ores exhibiting a positive correlation. Based on the above diagrams, it can be concluded that uranium (U) exhibits a significant positive correlation with trace elements such as molybdenum (Mo) and lead (Pb). Therefore, elements including Mo and Pb can be regarded as indicator elements for uranium enrichment.

6.2. Major Elements, pH and Eh Conditions and Mineralization

Uranium is a multivalent element that exists in two valence states, U6+ and U4+, under near-surface conditions. There are four main migration forms of uranium in supergene conditions: ① migration in the form of sulfate UO2SO4; ② migration in the form of uranyl carbonate complexes UO2(CO3)22−and [UO2(HCO3)64−; ③ migration in the form of soluble uranium–organic matter complexes; and ④ migration in the form of uranium colloidal solution [UO2(OH)2]. The sandstones of the Sifangtai Formation in the Daqing Placanticline area have a relatively high CaO content, with the average CaO content in uranium ores reaching 3.55%, which is 3.3 times that of the wall rocks and uranium-mineralized sandstones. It is thus inferred that uranium in the sandstone-type uranium deposits of the Daqing Placanticline may migrate in the form of uranyl carbonate ions. Due to changes in physicochemical conditions, the uranyl carbonate ions were decomposed, and the CO32− ions combined with Ca2+ ions to form carbonate minerals such as CaCO3. pH analysis of sandstones shows that uranium ores have lower pH values than host rocks and exhibit weak alkalinity, indicating that uranium mineralization occurred under conditions with a transition in acid–base properties. The Fe2O3/FeO ratio, total organic carbon (TOC) and total sulfur (∑S) contents also indicate that uranium enrichment is closely related to the content of reducing substances (e.g., organic matter, pyrite) in the rocks, with the mineralization occurring in a relatively strong reducing environment.

6.3. Trace Elements and Mineralization

Trace elements associated with typical interlayer oxidation zone-type uranium deposits and uranium mineralization include Se, Mo, Ge, Re, Sc and V. In contrast, the sandstone-type uranium deposits in the Daqing Placanticline are enriched in Mo and Pb, and relatively enriched in Zn, Sc, Y and other elements. It is evident that the element enrichment assemblage of the sandstone-type uranium deposits in the Daqing Placanticline differs from that of typical interlayer oxidation zone-type uranium deposits, which indicates that uranium mineralization is not solely driven by interlayer oxidation, but may also have been modified by late-stage fluids. Based on the spider diagrams of three types of sandstone samples (wall rocks, uranium-mineralized sandstones and uranium ores), the serrated variation amplitude of the spider curve for uranium ores increases, with the degree of relative enrichment or depletion of trace elements being significant. Combined with the geochemical characteristic that Y is relatively enriched in three samples and relatively depleted in the others, it is indicated that uranium enrichment is associated with late-stage (hydrothermal) reworking. Zr and Hf are high-field-strength and strongly mantle-affiliated elements, and their enrichment is mostly of endogenic deep-source origin. However, the sandstone samples in the study area are generally depleted in Zr and Hf, indicating that the late-stage mineralizing fluids should not be derived from the mantle. In addition, the northern Songliao Basin is rich in oil and gas resources; in particular, the Nenjiang Formation beneath the Sifangtai Formation serves as the major oil and gas reservoir. Moreover, the study area is well developed with faults, allowing the late-stage mineralizing fluids to incorporate the underlying oil and gas and superimpose reworking on the uranium orebodies. Late ore-forming fluids can mix with deep hydrocarbons and superimpose reworking on pre-existing uranium orebodies.

6.4. Rare Earth Elements and Mineralization

Rare earth elements (REE) have similar properties and geochemical behaviors, and usually participate in geological processes as a whole. In clastic rocks, REEs are mainly controlled by the rock compositions of provenance areas [54,55], and weathering and diagenesis have little effect on the redistribution of REEs [56]. REEs not only reflect the provenance of sedimentary mineralization and the source of fluids, but also can trace the traces of fluid activities [57,58]. Based on the rare earth element (REE) distribution patterns of wall rocks, mineralized sandstones and uranium ores from the sandstone-type uranium deposits in the Daqing Placanticline, all samples exhibit the characteristics of rightward inclination with light rare earth element (LREE) enrichment and insignificant heavy rare earth element (HREE) fractionation. In addition, the slope of the LREE segment is steeper than that of the HREE segment, which leads to the inference that these geological bodies share a common provenance, sedimentary environment and tectonic setting. Based on the correlation plots of total rare earth elements (ΣREE), light rare earth elements (LREE), heavy rare earth elements (HREE) versus uranium (U) for the samples, the rare earth element contents and the shapes of their distribution patterns are essentially consistent among wall rocks, mineralized sandstones and uranium ores. Some high-grade uranium ore samples (ZKMX02-ST3, ZKMX02-ST2) exhibit markedly elevated rare earth element (REE) contents with relative enrichment of heavy rare earth elements (HREE). Previous studies have demonstrated intense carbonatization within uranium ores, where minerals such as pyrite and calcite are commonly observed. This implies a high water/rock ratio. Such alteration may occur locally. It is therefore inferred that these high-grade uranium ore samples experienced modification by late ore-forming fluids.

6.5. Mineralization Model

The Sifangtai Formation represents a meandering river sedimentary formation. Its lower member belongs to the channel lag and point bar microfacies of the channel subfacies, where thick and large sand bodies with favorable porosity and permeability have developed. A set of stable mudstone–siltstone with a thickness of 35~55 m in the middle member of the Sifangtai Formation acts as the upper aquiclude, while the mudstone of the Nenjiang Formation underlying the Sifangtai Formation serves as the lower aquiclude. The interbedding of mudstone, sandstone and mudstone forms a favorable geological structure for sandstone-type uranium deposits. In the Daqing Placanticline area of the northern Songliao Basin, the regional tectonic stress increased since the Late Cretaceous, and subsidence was replaced by uplift, leading to the formation of inversion structures [59,60,61]. The strata above the Mingshui Formation were uplifted and denuded, forming tectonic denudation windows, which facilitated the infiltration of oxygen- and uranium-bearing water. Therefore, oxygen- and uranium-bearing water infiltrated into the high-porosity permeable sand bodies at the bottom of the Sifangtai Formation through the tectonic windows of the Chaoyanggou Anticline and the denudation windows of the Daqing Placanticline. Previous studies show that the δ13CPDB values of carbonate cements in the Sifangtai Formation range from −22.45‰ to −13.65‰, with an average of −18.33‰. The negative δ13CPDB signatures are likely caused by hydrocarbon fluids [62]. The underlying Quantou and Nenjiang Formations of the Sifangtai Formation serve as prolific hydrocarbon reservoirs. Abundant biogenic gas was generated at the end of Nenjiang Formation deposition, and large-scale hydrocarbon expulsion and hydrocarbon charging occurred at the end of the Mingshui Formation [63]. During this period, densely zoned faults developed in the southern Daqing Placanticline [64], which facilitated the migration and diffusion of deep hydrocarbon-bearing reducing fluids along faults [65]. These fluids mixed with oxygenated uranium-bearing fluids derived from the surface within sand bodies of the lower Sifangtai Formation and participated in uranium mineralization. Carbonate cements precipitated under weakly alkaline conditions and resulted in superimposed uranium enrichment (Figure 7).

7. Conclusions

Through an extensive analysis and discussion of the geochemical characteristics of the sandstone-type uranium deposits in the Daqing Placanticline of the northern Songliao Basin, the following conclusions are obtained:
  • Sandstones of the Sifangtai Formation exhibit distinct geochemical contrasts: uranium ores (mineralized sandstones) are enriched in total organic carbon and total sulfur and characterized by low Th/U and Fe2O3/FeO ratios, whereas host rocks show opposite features, indicating uranium enrichment under strongly reducing conditions. Elements including U, Pb and Mo are enriched during mineralization; Mo and Pb can be used as indicator elements for uranium mineralization. Uranium ores, mineralized sandstones and host rocks display similar REE distribution patterns, suggesting consistent provenance and sedimentary setting. Heavy rare earth element enrichment in high-grade ores records late fluid modification.
  • Combined with regional tectonics and hydrocarbon migration, sandstone-type uranium deposits in this area experienced two mineralization stages: supergene fluid mineralization and superimposed reworking by deep hydrocarbon-bearing reducing.

Author Contributions

Conceptualization, C.T.; methodology, C.T.; formal analysis, L.C. and Z.X.; investigation, H.L., J.W. and P.X.; data curation, L.C.; writing—original draft preparation, C.T.; writing—review and editing, C.T.; visualization, C.T. All authors have read and agreed to the published version of the manuscript.

Funding

This study is financially supported by the Deep Earth Probe and Mineral Resources Exploration–National Science and Technology Major Project (2025ZD1006800, 2025ZD1006805), the Project of China Geological Survey (DD20240116) and the APC was funded by DD20240116.

Data Availability Statement

Data is contained within the article.

Acknowledgments

We are grateful to all participants of this project for their support in field sampling, laboratory analysis and data processing. We greatly appreciate the comments from editors and anonymous reviewers, which have highly improved the quality of this manuscript.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Tectonic division map of the Songliao Basin and the study area. (a) Structural map of northeast China showing the distribution of Mesozoic and Cenozoic sedimentary basins (modified after Bonnetti et al., 2015 [40]). (b) Tectonic map of the Songliao Basin (modified after Liu et al., 2026 [41]). (c) Tectonic division Map of the Daqing Placanticline area, showing the locations of some drillholes and Profile L1 (modified after Tangchao et al., 2021 [19]). BB = Bohai Basin, EB = Erlian Basin, EGB = East Gobi Basin, HB = Hailar Basin, OB = Ordos Basin, SB = Songliao Basin, YB = Yingen Basin, BL = Baikal Lake, MOZ = Mongol-Okhotsk Zone.
Figure 1. Tectonic division map of the Songliao Basin and the study area. (a) Structural map of northeast China showing the distribution of Mesozoic and Cenozoic sedimentary basins (modified after Bonnetti et al., 2015 [40]). (b) Tectonic map of the Songliao Basin (modified after Liu et al., 2026 [41]). (c) Tectonic division Map of the Daqing Placanticline area, showing the locations of some drillholes and Profile L1 (modified after Tangchao et al., 2021 [19]). BB = Bohai Basin, EB = Erlian Basin, EGB = East Gobi Basin, HB = Hailar Basin, OB = Ordos Basin, SB = Songliao Basin, YB = Yingen Basin, BL = Baikal Lake, MOZ = Mongol-Okhotsk Zone.
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Figure 3. Element content distribution curves for different sandstone types of the Sifangtai Formation in the Daqing Placanticline area.
Figure 3. Element content distribution curves for different sandstone types of the Sifangtai Formation in the Daqing Placanticline area.
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Figure 4. The standard spider web diagram of trace elements of Chinese sedimentary rocks in sandstone of Sifangtai Formation in the Daqing Placanticline area (standardized data from Litong, 1994 [52]). (a)—wall rock; (b)—uranium-mineralized sandstone; (c)—uranium ore.
Figure 4. The standard spider web diagram of trace elements of Chinese sedimentary rocks in sandstone of Sifangtai Formation in the Daqing Placanticline area (standardized data from Litong, 1994 [52]). (a)—wall rock; (b)—uranium-mineralized sandstone; (c)—uranium ore.
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Figure 5. The standardized distribution map of rare earth element chondrites in sandstone of Sifangtai Formation in the Daqing Placanticline are staandardized data from Taylor and Mclennan, 1985 [53]. (a)—wall rock; (b)—uranium-mineralized sandstone; (c)—uranium ore.
Figure 5. The standardized distribution map of rare earth element chondrites in sandstone of Sifangtai Formation in the Daqing Placanticline are staandardized data from Taylor and Mclennan, 1985 [53]. (a)—wall rock; (b)—uranium-mineralized sandstone; (c)—uranium ore.
Minerals 16 00953 g005
Minerals 16 00953 g006
Figure 6. Log-log correlation diagrams of uranium and other elements in sandstone-type uranium ore from the Daqing Placanticline, Northern Songliao Basin. (a) Th-U correlation diagram; (b) Th/U-U correlation diagram; (c) Mo-U corelation diagram; (d) Pb-U corelation diagram; (e) Sc-U correlation diagram; (f) Y-U correlation diagram; (g) ∑REE-U corelation diagram; (h) LREE-U corelation diagram; (i) HREE-U corelation diagram.
Figure 6. Log-log correlation diagrams of uranium and other elements in sandstone-type uranium ore from the Daqing Placanticline, Northern Songliao Basin. (a) Th-U correlation diagram; (b) Th/U-U correlation diagram; (c) Mo-U corelation diagram; (d) Pb-U corelation diagram; (e) Sc-U correlation diagram; (f) Y-U correlation diagram; (g) ∑REE-U corelation diagram; (h) LREE-U corelation diagram; (i) HREE-U corelation diagram.
Minerals 16 00953 g006
Minerals 16 00953 g007
Figure 7. Metallogenic model diagram of uranium in the Daqing Placanticline area, Northern Songliao Basin.
Figure 7. Metallogenic model diagram of uranium in the Daqing Placanticline area, Northern Songliao Basin.
Minerals 16 00953 g007
Table 1. Samples and their lithological characteristics of sandstone-type uranium deposit in Daqing Placanticline, northern Songliao Basin.
Table 1. Samples and their lithological characteristics of sandstone-type uranium deposit in Daqing Placanticline, northern Songliao Basin.
No.Sample TypeSample No.Drillhole IDSample Depth (m)Lithology
1Wall RockDX00-01-9ZKDX00394.43Motley argillaceous siltstone
2DX00-01-6ZKDX00391.83Grayish-red argillaceous siltstone
3CD06-2ZKCD06299.00Light-grayish-green medium sandstone
4DX00-01-33ZKDX00418.02Light-gray fine sandstone
5DX00-01-18ZKDX00403.68Light-grayish-green fine sandstone
6DX00-01-42ZKDX00416.92Light-red fine sandstone
711D35-1-22911D35-1231.00Gray siltstone
8DX00-01-15ZKDX00404.68Light-greenish-gray fine sandstone
9DX00-01-12ZKDX00405.68Light-greenish-gray fine sandstone
10DX00-01-39ZKDX00415.55Light-red gravel-bearing fine sandstone
11168D-2-ST1168D-2233.00Greenish-gray argillaceous siltstone
12ZKCD13-1ZKCD13270.00Grayish-green fine sandstone
13ZKCD15-1ZKCD15272.00Gray medium sandstone
14ZKCD06-3ZKCD06306.00Light-gray medium sandstone
1511D35-1-24011D35-1236.00Gray fine sandstone
16DX00-01-21ZKDX00407.85Light-grayish-green fine sandstone
17DX00-01-30ZKDX00414.05Light-gray fine sandstone
18Uranium-mineralized
sandstone		MX02-ST1ZKMX02257.00Light-gray medium sandstone
19CD06-1ZKCD06295.00Light-gray medium sandstone
20TT16-ST1ZKTT16203.00Light-gray fine sandstone
21166D-1-ST1166D-1220.00Light-gray medium sandstone
22MX06-YS2ZKMX06206.80Gray medium sandstone
2311D35-1-23711D35-1234.00Gray fine sandstone
24Uranium OreMX06-ST3ZKMX06224.00Gray fine sandstone
25TT16-ST3ZKTT16215.00Light-gray medium sandstone
26TT16-ST2ZKTT16212.00Light-gray medium sandstone
27168D-3-ST3168D-3207.00Gray fine sandstone
28166D-1-ST3166D-1230.00Light-gray fine sandstone
29DX00-01-24ZKDX00409.35Light-gray ore-bearing fine sandstone
30166D-1-ST2166D-1228.00Light-gray medium sandstone
31MX06-ST2ZKMX06222.00Gray fine sandstone
32DX00-01-27ZKDX00410.25Light-gray ore-bearing fine sandstone
33MX06-ST1ZKMX06220.00Gray fine sandstone
34168D-3-ST2168D-3205.00Gray fine sandstone
35CD08-YS1ZKCD08247.50Gray fine sandstone
36168D-2-ST3168D-2237.00Dark-gray argillaceous siltstone
37168D-3-ST1168D-3204.00Gray fine sandstone
3811D35-1-23211D35-1233.00Gray fine sandstone
39168D-2-ST2168D-2235.00Dark-gray argillaceous siltstone
40MX02-ST3ZKMX02252.00Dark-gray argillaceous siltstone
41MX02-ST2ZKMX02255.00Light-gray medium sandstone
Table 2. Major element analysis results of sandstone samples from the Sifangtai Formation in the Daqing Placanticline area (×10−2).
Table 2. Major element analysis results of sandstone samples from the Sifangtai Formation in the Daqing Placanticline area (×10−2).
No.Sample No.ThUTh/USiO2Al2O3Fe2O3FeOMgOCaONa2OK2OMnOTiO2P2O5Loss on IgnitionFe2O3/FeO
1DX00-01-911.501.916.0265.5214.603.420.621.501.062.502.270.030.540.068.165.52
2DX00-01-612.302.345.2663.0414.705.890.511.351.032.392.560.130.710.118.1411.55
3CD06-23.682.601.4277.7511.630.800.480.491.112.882.610.020.280.041.901.67
4DX00-01-334.433.431.2980.479.680.820.670.391.012.312.240.020.310.042.121.23
5DX00-01-185.353.531.5276.5211.321.320.470.571.112.572.530.020.310.043.352.81
6DX00-01-423.184.050.7981.818.810.930.420.340.902.032.320.010.150.042.282.22
711D35-1-22913.004.213.0964.8314.344.131.461.281.182.272.590.060.660.077.492.83
8DX00-01-154.424.231.0478.8810.520.980.520.450.992.492.550.010.240.042.391.88
9DX00-01-123.385.020.6783.398.390.530.420.320.731.972.330.010.140.041.761.27
10DX00-01-393.635.400.6780.009.661.170.420.410.952.262.280.010.190.042.662.78
11168D-2-ST110.405.881.7768.8014.043.710.511.191.272.372.470.040.580.065.297.28
12CD13-11.637.870.2172.9712.921.760.640.941.312.842.580.030.420.143.542.74
13CD15-12.109.270.2375.9412.051.510.350.621.222.942.570.040.600.062.214.32
14CD06-35.6111.600.4877.7411.770.560.750.510.922.782.480.020.410.051.970.74
1511D35-1-24012.7013.000.9865.7214.643.930.501.361.182.262.700.060.610.057.347.87
16DX00-01-213.8614.400.2780.219.640.780.440.401.192.222.410.040.210.052.501.77
17DX00-01-304.3714.700.3079.569.950.810.660.480.952.252.300.010.210.042.841.23
Average6.216.671.5374.8911.691.940.580.741.072.432.460.030.390.063.883.51
18MX02-ST16.3722.000.2975.5812.620.920.430.751.202.882.480.030.350.052.732.14
19CD06-19.8829.300.3469.5514.612.140.651.241.102.632.630.040.610.084.873.30
20TT16-ST14.2531.300.1481.279.890.490.440.420.932.342.500.020.220.041.451.11
21166D-1-ST14.1750.500.0880.3610.290.320.390.400.962.502.770.020.190.041.760.83
22MX06-YS213.4055.800.2467.5514.132.001.091.291.102.722.270.030.540.087.351.83
2311D35-1-2375.5896.200.0679.2910.840.470.460.421.162.492.540.020.280.051.931.03
Average7.2847.520.1975.6012.061.060.580.751.082.592.530.030.360.053.351.71
24MX06-ST36.52103.000.0677.7111.700.540.570.601.072.722.680.020.270.052.040.96
25TT16-ST34.15105.000.0480.9010.010.410.430.440.962.342.530.020.200.041.670.96
26TT16-ST24.81119.000.0480.9510.040.440.410.420.942.322.570.020.190.041.601.08
27168D-3-ST36.56127.000.0575.1412.331.320.450.781.112.632.580.040.390.063.222.94
28166D-1-ST33.64133.000.0354.447.600.220.430.3917.241.781.951.160.190.0514.570.52
29DX00-01-243.90138.000.0379.2610.420.350.520.421.172.492.530.030.210.062.530.67
30166D-1-ST24.74157.000.0360.048.070.140.390.3914.351.932.050.490.210.0511.890.37
31MX06-ST28.42175.000.0574.4213.070.970.530.891.242.862.490.040.330.073.101.82
32DX00-01-274.20232.000.0278.4811.040.400.570.451.122.552.590.020.270.082.460.69
33MX06-ST16.60246.000.0374.8612.880.840.520.801.192.872.670.030.250.073.091.62
34168D-3-ST28.27282.000.0371.9412.851.690.571.061.142.522.450.050.430.085.302.96
35CD08-YS112.20325.000.0466.5413.172.341.251.122.112.622.140.180.400.088.011.88
36168D-2-ST38.09339.000.0265.1811.872.270.830.855.942.292.170.610.450.077.612.73
37168D-3-ST17.46446.000.0270.7312.391.990.941.011.132.482.420.050.400.086.532.12
3811D35-1-23210.60517.000.0267.6212.572.870.541.001.322.472.220.050.430.108.525.31
39168D-2-ST27.031140.000.0164.8712.020.800.950.876.572.332.150.650.400.098.320.84
40MX02-ST312.503484.000.00460.2016.071.703.591.861.462.112.900.110.630.479.040.47
41MX02-ST27.824974.000.00266.7512.780.482.631.083.842.302.580.360.440.466.320.18
Average7.08724.560.0370.5611.721.100.900.803.552.422.430.220.340.115.881.56
Fe2O3 = TFe2O3 − 1.11 × FeO.
Table 3. Trace element analysis results of sandstone samples from the Sifangtai Formation in the Daqing Placanticline area (×10−6).
Table 3. Trace element analysis results of sandstone samples from the Sifangtai Formation in the Daqing Placanticline area (×10−6).
No.Sample NoCsPbThUCuZnMoBaVCoNiCrGaRbSrNbTaZrHfYSc
1DX00-01-98.3219.611.51.9122.164.90.36554751.610.7018.9046.318.0102.028414.401.080129.03.9424.99.61
2DX00-01-612.9023.512.32.3413.680.70.55361572.112.3021.5050.019.6129.026416.101.180139.04.1621.412.90
3CD06-22.7012.23.682.617.722.50.85362327.03.076.2321.212.379.02586.280.45246.31.4210.43.68
4DX00-01-332.6411.64.433.4314.921.60.28654230.34.136.4924.211.872.82426.740.43154.51.3812.44.13
5DX00-01-183.0212.95.353.5312.430.90.26861831.04.647.9328.413.184.92867.570.52370.11.9612.65.11
6DX00-01-422.5610.23.184.057.716.90.19554017.23.125.4813.510.076.12144.070.28945.71.2410.73.05
711D35-1-22912.810.013.004.2119.760.90.35581991.29.8720.2048.518.712025916.401.380131.03.9330.411.2
8DX00-01-152.6612.14.424.239.1622.90.26559826.63.366.0920.012.081.22565.770.43355.51.5310.53.90
9DX00-01-122.1910.13.385.027.6315.90.22155217.62.324.3412.69.4974.02034.020.30445.21.289.92.72
10DX00-01-392.6910.73.635.406.1920.80.24155220.53.536.1419.211.275.12415.260.40448.71.3410.93.69
11168D-2-ST18.2517.910.405.8823.759.41.97066773.19.5313.2052.217.4108.027513.300.97496.83.1720.810.2
12CD13-15.4815.01.637.8714.840.00.54169346.37.2911.3032.514.992.22739.480.75685.42.7528.36.70
13CD15-13.7016.52.109.2717.741.40.60463855.76.249.8648.413.782.925911.200.88893.73.0516.15.82
14CD06-33.0356.05.6111.6011.730.50.77458441.514.5015.4042.412.877.52257.660.57368.52.1511.15.61
1511D35-1-24011.617.012.713.0017.569.24.69094260.911.6017.2048.519.0127.028214.701.320118.03.8221.311.10
16DX00-01-212.2911.03.8614.4014.416.80.26855920.65.445.4316.111.076.92324.840.36249.91.3810.33.52
17DX00-01-302.7210.44.3714.705.320.30.23455424.23.865.7118.411.675.92425.570.41355.01.489.94.21
18MX02-ST12.8117.56.3722.00232.028.00.71054155.613.4010.6031.014.077.62658.160.65958.11.9110.55.71
19CD06-17.8026.69.8829.3022.989.61.950213654.314.2016.5055.018.0106.026314.101.160104.03.4622.79.88
20TT16-ST12.3414.34.2531.307.4922.30.74076323.96.006.7817.310.973.42135.810.47839.61.3311.13.39
21166D-1-ST12.2320.24.1750.506.1614.415.20065522.025.7014.8015.010.877.22184.250.34836.11.219.02.95
22MX06-YS27.4826.613.455.8023.888.58.26045472.923.5023.5037.521.1143.028712.301.160100.03.6421.38.02
2311D35-1-2372.5115.75.5896.204.220.619.80071623.65.316.3317.812.072.72516.850.61457.31.8410.23.75
24MX06-ST32.8617.96.52103.0014.232.44.05058826.615.4013.4021.413.179.02527.890.72649.81.6715.24.03
25TT16-ST32.3515.14.15105.006.819.81.24069321.55.977.1416.111.074.52145.350.49939.51.3111.03.39
26TT16-ST22.4216.24.81119.006.922.41.27069920.96.798.5114.011.477.52265.440.49139.71.3612.23.39
27168D-3-ST33.0917.36.56127.0010.136.967.20061235.36.489.6830.413.577.92348.770.72765.62.1414.15.36
28166D-1-ST31.781583.64133.009.365.617.7049817.632.6021.0010.09.161.72684.370.35132.11.0212.83.78
29DX00-01-242.2614.53.90138.005.921.40.28858427.517.1011.7016.911.882.02465.090.37854.41.369.953.80
30166D-1-ST21.6635.84.74157.005.720.69.16050620.519.1016.7018.48.759.82794.500.37231.00.9913.83.47
31MX06-ST23.5022.78.42175.0010.536.12.34054427.822.9017.1024.415.577.728510.301.12060.62.1514.55.53
32DX00-01-272.3914.14.20232.004.317.00.30359929.99.027.5820.212.779.22636.290.44158.81.5410.14.80
33MX06-ST13.2919.96.60246.0013.431.53.13059928.517.7014.5019.114.578.82698.081.06049.31.7413.34.94
34168D-3-ST23.5820.38.27282.00437.0169.056.30089838.111.0012.1035.614.979.52439.700.85876.32.5116.46.81
35CD08-YS14.2324.412.20325.0017.472.51459.00047733.46.7511.7027.018.7117.027813.201.34092.53.2635.76.06
36168D-2-ST33.9321.88.09339.0015.288.9109.00059041.416.320.8030.513.572.02578.920.69772.12.3216.67.09
37168D-3-ST13.3821.27.46446.0013.659.5226.00061542.511.0012.9034.714.576.32319.520.78975.22.3023.97.86
3811D35-1-2324.5739.610.60517.0015.071.52237.00084349.59.3218.5032.816.277.129611.401.090108.03.4714.97.54
39168D-2-ST23.51114.07.031140.0013.9153.070.80061036.415.6023.3028.513.370.12698.670.70068.52.2017.76.49
40MX02-ST39.7559.712.503484.0034.2139.01984.000395105.032.1043.0065.223.4122.024313.200.99798.83.1432.414.1
41MX02-ST25.44357.07.824974.002464.050.3556.00049298.1440.00270.0038.517.391.62449.780.72976.32.4451.49.14
Chinese Sedimentary Rocks [52]6.9011.08.702.0028.045.00.56026054.033.0025.0052.013.095.03309.900.900130.03.9020.010.00
Table 4. Rare earth element analysis results of sandstone samples from the Sifangtai Formation in the Daqing Placanticline area (×10−6).
Table 4. Rare earth element analysis results of sandstone samples from the Sifangtai Formation in the Daqing Placanticline area (×10−6).
No.Sample No.LaCePrNdSmEuGdTbDyHoErTmYbLuREELREEHREELREE/HREE(La/Yb)NLa/SmGd/YbEuCe
1DX00-01-936.468.38.0230.05.581.1404.910.8244.360.8332.390.3992.550.38166.086149.44016.6468.989.65 4.11 1.56 0.67 0.94
2DX00-01-630.855.66.4523.34.050.8133.530.6053.420.7052.180.3832.610.39134.836121.01313.8238.757.97 4.79 1.10 0.66 0.92
3CD06-221.540.64.6917.43.140.7182.610.4112.000.3841.020.1871.150.16295.97288.0487.92411.1112.63 4.31 1.84 0.77 0.95
4DX00-01-3325.449.55.4419.43.170.8222.550.4402.110.3941.090.1841.130.162111.792103.7328.06012.8715.19 5.04 1.83 0.88 0.99
5DX00-01-1822.241.24.6317.02.790.7242.500.4042.100.4001.190.2021.200.17596.71588.5448.17110.8412.50 5.01 1.69 0.84 0.95
6DX00-01-4219.739.14.3816.72.720.7002.350.3801.920.3440.990.1560.9510.13790.53083.3007.23011.5214.00 4.56 2.00 0.85 0.99
711D35-1-22941.379.29.2735.76.611.3306.061.0605.671.0903.110.5603.370.496194.826173.41021.4168.108.28 3.93 1.46 0.64 0.95
8DX00-01-1519.937.54.1315.62.60.6442.150.3581.940.3320.940.1551.020.14487.41180.3747.03711.4213.18 4.82 1.71 0.83 0.97
9DX00-01-1219.839.24.3316.12.840.7312.410.3741.830.3380.910.1400.900.13290.03283.0017.03111.8114.92 4.39 2.18 0.85 0.99
10DX00-01-3919.337.24.1915.32.790.6762.280.3731.890.3550.950.1660.990.1586.61179.4567.15511.1013.16 4.35 1.86 0.82 0.97
11168D-2-ST133.263.27.3027.14.931.0304.410.7253.720.7482.060.3782.460.347151.608136.7614.8489.219.12 4.24 1.45 0.68 0.95
12CD13-128.556.46.5225.15.181.1904.630.8664.520.9442.410.4202.560.37139.610122.89016.7207.357.52 3.46 1.47 0.74 0.97
13CD15-131.657.46.6624.44.240.8843.480.5592.870.5501.550.2801.780.249136.502125.18411.31811.0612.00 4.69 1.58 0.70 0.93
14CD06-323.144.15.0618.43.20.7802.590.4242.060.3991.120.2001.310.186102.92994.6408.28911.4211.92 4.54 1.60 0.83 0.96
1511D35-1-24037.2738.0931.05.471.1204.690.7633.990.8132.410.4372.750.407172.14155.88016.2609.599.14 4.28 1.38 0.68 0.99
16DX00-01-2120.2384.3716.12.620.6702.220.3561.790.3290.900.1390.990.13288.81281.9606.85211.9613.82 4.85 1.82 0.85 0.95
17DX00-01-3021.942.34.5616.82.890.6812.320.3641.740.3250.880.1550.970.13896.02289.1316.89112.9315.29 4.77 1.94 0.80 0.99
18MX02-ST120.740.34.5916.93.120.7662.470.4102.010.3871.080.1971.240.17194.34186.3767.96510.8411.28 4.18 1.61 0.84 0.97
19CD06-136.568.28.0229.85.571.1804.740.8134.050.7842.180.3902.480.356165.063149.27015.7939.459.95 4.12 1.55 0.70 0.93
20TT16-ST120.140.74.4016.42.960.7362.420.4232.070.3791.060.2001.220.16493.23285.2967.93610.7511.13 4.27 1.61 0.84 1.01
21166D-1-ST121.340.84.5116.72.910.7182.420.3711.800.320.900.1530.960.13193.99686.9387.05812.3214.93 4.61 2.03 0.83 0.98
22MX06-YS229.856.66.7425.24.720.8894.060.743.970.802.350.4342.720.396139.419123.94915.4708.017.40 3.97 1.21 0.62 0.94
2311D35-1-23723.744.85.0318.93.280.8522.780.4482.260.4191.160.1991.250.172105.25096.5628.68811.1112.81 4.55 1.80 0.86 0.96
24MX06-ST319.238.94.4116.13.240.7382.710.5112.710.5321.440.2601.720.23192.70282.58810.1148.177.54 3.73 1.28 0.76 0.99
25TT16-ST318.336.83.9514.72.770.6622.260.3781.850.3691.020.1781.100.1684.49777.1827.31510.5511.24 4.16 1.67 0.81 1.01
26TT16-ST220.940.84.5016.53.030.7012.420.4192.100.4171.130.2111.310.18594.62386.4318.19210.5510.78 4.34 1.50 0.79 0.99
27168D-3-ST321.540.34.8018.13.430.8022.910.5152.680.5311.410.2571.640.22899.10388.93210.1718.748.86 3.95 1.44 0.78 0.93
28166D-1-ST315.831.23.4813.42.410.5652.170.3731.950.3981.100.2081.270.18374.50766.8557.6528.748.41 4.13 1.38 0.76 0.99
29DX00-01-2417.833.63.8713.82.380.6692.120.3401.780.3110.900.1420.9640.12978.79472.1196.67510.8012.48 4.71 1.78 0.91 0.95
30166D-1-ST223.444.34.9618.53.290.6662.800.4752.280.4621.280.2341.390.208104.24595.1169.12910.4211.38 4.48 1.63 0.67 0.96
31MX06-ST21835.13.9914.42.820.6572.430.4472.450.4821.330.2521.600.22384.18174.9679.2148.147.60 4.02 1.23 0.77 0.97
32DX00-01-2719.436.94.0215.22.620.6422.230.3501.750.3210.940.1441.010.13685.66378.7826.88111.4512.98 4.66 1.79 0.81 0.98
33MX06-ST117.432.43.7113.62.810.6572.330.4322.330.4771.270.241.560.22379.43970.5778.8627.967.54 3.90 1.21 0.78 0.94
34168D-3-ST227.951.35.9521.23.950.8023.320.5592.770.5441.470.2831.770.254122.072111.10210.97010.1310.65 4.45 1.52 0.68 0.93
35CD08-YS133.663.57.5830.06.001.0505.611.0706.281.2803.600.6523.830.559164.611141.73022.8816.195.93 3.52 1.19 0.55 0.93
36168D-2-ST333.567.18.0229.75.761.154.640.8003.980.7411.990.3582.300.323160.362145.23015.1329.609.84 3.66 1.64 0.68 0.96
37168D-3-ST131.155.86.5425.34.750.8553.960.7003.580.7692.140.392.480.347138.711124.34514.3668.668.47 4.12 1.29 0.60 0.92
3811D35-1-23225.345.95.420.73.970.9583.370.6433.460.6671.870.3422.180.301115.061102.22812.8337.977.84 4.01 1.25 0.80 0.92
39168D-2-ST224.845.65.2319.03.650.8353.060.5342.820.5801.650.3042.000.289110.35299.11511.2378.828.38 4.28 1.24 0.76 0.94
40MX02-ST350.997.810.940.07.151.4106.461.1105.671.0802.880.5083.150.421229.439208.16021.2799.7810.92 4.48 1.66 0.63 0.97
41MX02-ST243.673.38.1731.15.751.1905.380.9965.421.2603.660.6864.310.664185.486163.11022.3767.296.84 4.77 1.01 0.65 0.91
chondrite [53]0.3670.9570.1370.7110.2310.0870.3060.0580.3810.08510.2490.03560.2480.03813.8912.4901.4011.781.001.00 1.00 1.00 1.00
Table 5. Statistical table of geochemical index parameters of sandstones of the Sifangtai Formation in the Daqing Placanticline area.
Table 5. Statistical table of geochemical index parameters of sandstones of the Sifangtai Formation in the Daqing Placanticline area.
CategoryU/10−6Fe3+/Fe2+CTOC/10−6Stotal/10−6S2−/10−6pHEh /mV
Wall rock (n = 20)7.152.310.160.040.019.76367.50
Uranium-mineralized sandstone (n = 54)53.271.560.220.240.039.55375.12
Uranium ore (n = 35)314.711.440.330.400.039.56366.56
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Tang, C.; Chen, L.; Xu, Z.; Liu, H.; Wei, J.; Xiao, P. Geochemical Characteristics of Sandstone-Type Uranium Deposits and Their Significance for Uranium Mineralization in Daqing Placanticline, Northern Songliao Basin. Minerals 2026, 16, 953. https://doi.org/10.3390/min16090953

AMA Style

Tang C, Chen L, Xu Z, Liu H, Wei J, Xiao P. Geochemical Characteristics of Sandstone-Type Uranium Deposits and Their Significance for Uranium Mineralization in Daqing Placanticline, Northern Songliao Basin. Minerals. 2026; 16(9):953. https://doi.org/10.3390/min16090953

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Tang, Chao, Lulu Chen, Zenglian Xu, Huajian Liu, Jialin Wei, and Peng Xiao. 2026. "Geochemical Characteristics of Sandstone-Type Uranium Deposits and Their Significance for Uranium Mineralization in Daqing Placanticline, Northern Songliao Basin" Minerals 16, no. 9: 953. https://doi.org/10.3390/min16090953

APA Style

Tang, C., Chen, L., Xu, Z., Liu, H., Wei, J., & Xiao, P. (2026). Geochemical Characteristics of Sandstone-Type Uranium Deposits and Their Significance for Uranium Mineralization in Daqing Placanticline, Northern Songliao Basin. Minerals, 16(9), 953. https://doi.org/10.3390/min16090953

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