Paleoproterozoic U Mineralization in Huayangchuan Deposit, Xiaoqinling Area: Evidence from the U–Rich Granitic Pegmatite

: The Huayangchuan uranium deposit, located in the west of the Xiaoqinling belt on the southern margin of the North China Craton, is a large U–Nb–Pb deposit accompanied with rare–earth elements. The Huayangchuan uranium deposit, discovered in the 1950s


Introduction
The Huayangchuan U deposit in the Qinling Orogenic Belt (Central China; QLOB) was discovered during the 1950s. In the last decade, the Huayangchuan deposit has been recognized as a large U-Nb-Pb deposit accompanied with REE [1][2][3]. Since its discovery, it has been famous worldwide for the rare presence of carbonate veins rich in U, Nb, Pb, and REE [4][5][6]. Many studies have been published on carbonatites in Huayangchuan, including their chronology, petrography, and geochemistry, all of which point to an igneous origin of carbonatites in QLOB in the evolutionary background of the Late Triassic [7][8][9][10][11][12][13]. Apart from Huayangchuan, the district also contains other large deposits, such as the Xigou carbonatite-related Mo deposit and Huanglongpu carbonatite-related Mo-Pb(-Re) deposit. Regionally, these typical deposits are part of the Triassic carbonatite metallogenic belt of North Qinling.  [2]).
According to the metallogenic characteristics of uranium in the area, the geological bodies closely related to uranium mineralization mainly include the Taihua group, Huayangchuan fault zone, and Laoniushan and Huashan granites. Local stratigraphic units in the Huayangchuan area comprise the Archean Taihua group, which is a high-grade metamorphosed and the main outcropping sequence. The Taihua group provided magma Minerals 2023, 13, 936 3 of 23 sources and materials for various crystallization and mineralization events. Major faults (e.g., Taiyao, Xiaohe, Huayangchuan, and Luonan-Luanchuan; Figure 1c) are all NE-or EWtrending, superimposed by NS-trending secondary faults and fractures. The NE-trending Huayangchuan Fault controls the major distribution of ore bodies in Huayangchuan. In Huayangchuan, the magmatic rocks mainly comprise Proterozoic granite and pegmatite, Triassic carbonatite dikes, and Jurassic-Cretaceous granitoids ( Figure 2).

Characteristics of U-rich Granitic Pegmatite and Sample Collection
Many U-rich granitic pegmatite veins have been found in the western area of the Huayangchuan deposit. Field observations showed that the U-rich granitic pegmatite veins intruded into the Taihua group (Figure 3a,b). Its width can generally reach 1-3 m; length can reach at least 100 m. Its extension direction is nearly E-W, and the dip angle is approximately 50°-70°. The chloritization and weathering of the contact zone formed by Figure 2. Simplified geologic map of the Huayangchuan deposit (modified from [13]).

Characteristics of U-Rich Granitic Pegmatite and Sample Collection
Many U-rich granitic pegmatite veins have been found in the western area of the Huayangchuan deposit. Field observations showed that the U-rich granitic pegmatite veins intruded into the Taihua group (Figure 3a,b). Its width can generally reach 1-3 m; length can reach at least 100 m. Its extension direction is nearly E-W, and the dip angle is approximately 50 • -70 • . The chloritization and weathering of the contact zone formed by the U-rich granite pegmatite and the surrounding rock were evident (Figure 3a,b), indicating that the contact zone was a weak area where fluids could easily act. The U contents in some granitic pegmatite veins can reach high industrial grade. Some U-rich granitic pegmatite veins can also be observed deep underground through drilling. the U-rich granite pegmatite and the surrounding rock were evident (Figure 3a,b), indicating that the contact zone was a weak area where fluids could easily act. The U contents in some granitic pegmatite veins can reach high industrial grade. Some U-rich granitic pegmatite veins can also be observed deep underground through drilling. The studied pegmatite samples were collected from the western Huayangchuan deposit ( Figure 2). Two groups of typical representative U-rich granitic pegmatite samples were tested for petrography, mineralogy, whole-rock geochemistry, zircon U-Pb ages, and in situ Lu-Hf isotopes.

Petrography and Mineralogy Analysis
Petrography and mineralogy analysis of U-rich granitic pegmatite slice samples were conducted at the Xi'an Center of Geological Survey, CGS (China), to study the microscopic characteristics and mineral compositions. A German Zeiss Stemi 305 polarizing micro-  The studied pegmatite samples were collected from the western Huayangchuan deposit ( Figure 2). Two groups of typical representative U-rich granitic pegmatite samples were tested for petrography, mineralogy, whole-rock geochemistry, zircon U-Pb ages, and in situ Lu-Hf isotopes.

Petrography and Mineralogy Analysis
Petrography and mineralogy analysis of U-rich granitic pegmatite slice samples were conducted at the Xi'an Center of Geological Survey, CGS (Xi'an, China), to study the microscopic characteristics and mineral compositions. A German Zeiss Stemi 305 polarizing microscope was used to observe the microscopic characteristics (in cross-polarized light) of U-rich granitic pegmatites samples. And then, an MLA650 scanning electron microscopy (SEM) was used for mineral composition analysis.

Zircon U-Pb Geochronology
Zircon crystals were separated using heavy-liquid and magnetic methods. Separated zircons were carefully handpicked under a binocular microscope. The selected high-quality zircons were further mounted in epoxy resins and finally polished to approximately half their thickness for analysis. CL images were captured at the Xi'an Center of Geological Survey, CGS (China), to investigate internal structures of analyzed zircons and to select target positions for U-Pb dating analysis. Zircon U-Pb analyses were performed at the Key Laboratory for the Study of Focused Magmatism and Giant Ore Deposits, MLR, Xi'an Center of Geological Survey, China Geological Survey (CGS), using an Agilent 7700× ICP-MS coupled with a 193 nm ArFexcimer laser ablation system (Geolas Pro). A 32 µm spot size and 9 Hz energy density were adopted. Each analysis incorporated a background acquisition time of approximately 20 s (gas blank) followed by 40 s of data acquisition during the ablation. The ratios of U-Th-Pb were calculated using Glitter 4.4 and were corrected for both instrumental mass bias and depth dependent elemental and isotopic fractionation using a Harvard standard zircon 91500. Concordia diagrams and weighted mean calculations were carried out using Isoplot/Ex. 3 software [16]. Common Pb compositions were calibrated using the method described by Andersen [17]. Trace element compositions of zircons were calibrated against reference materials (NIST610), which were combined with Si as internal standardization.

Major and Trace Element Analyses
Twenty essentially fresh whole-rock samples from four groups were collected for major and trace element analyses, including ten U-rich granitic pegmatites, five surrounding rock samples from the Taihua group, and five granite samples of Huashan pluton. Major-and trace-element analyses were performed at the Key Laboratory for the Study of Focused Magmatism and Giant Ore Deposits in Xi'an, (China). Whole-rock geochemical analyses were performed using X-ray fluorescence (XRF) and ICP-MS, with analytical errors < 3 wt.% for most elements. Loss on ignition (LOI) was estimated using an electronic analytical balance at constant temperature of approximately 1000 • C. The detailed procedures followed are as described by Yang et al. [18].

Zircon Hf Isotopic Analyses
Zircon Lu-Hf isotope measurements were performed using a Geolas-Pro laser ablation system coupled to a Neptune multiple-collector inductively coupled plasma mass spectrometry (ICP-MS). Details of the instrumental conditions and acquisition were similar to those described in previous studies [19]. A stationary laser ablation spot with a beam diameter of 32 µm was used for the analyses. During the analysis, zircon GJ-1 was used as the reference standard, yielding a weighted mean 176 Hf/ 177 Hf ratio of 0.281990-0.282070. The present-day chondritic ratios of 176 Hf/ 177 Hf and 176 Lu/ 177 Hf are 0.282772 and 0.0332 [20], respectively. The decay constant for 176 Lu is 1.865 × 10 −11 a −1 [21]; these values were The U-rich granitic pegmatites are mainly composed of quartz (approximately 15-25 wt.%), K-feldspar (mainly microcline is characterized by tartan twinning, approximately 50-60 wt.%), plagioclase (approximately 10-20 wt.%), and small amounts of biotite, hornblende, and accessory minerals. Its total mineral composition was approximately equivalent to that of granite. The contact boundary formed by gneissic xenoliths of the Taihua group in the U-rich granitic pegmatites was observed under a polarizing microscope (Figure 4a). The rock-forming minerals of the U-rich granitic pegmatites exhibited an evidently coarse pegmatitic texture (Figure 4b). In addition, zircon particles can be observed between the inter-crystalline fractures of K-feldspar and quartz ( Figure 4c). Meanwhile, intrusion of quartz veinlets into the plagioclase fissure of gneiss was observed (Figure 4d), suggesting that the magmatic hydrothermalism occurred during the formation of U-rich granitic pegmatite.

Characteristics of Principal Uranium Minerals and Zircon
Scanning electron microscopy (SEM) showed that the main uranium minerals in the U-rich granitic pegmatite are betafite and uraninite. The paragenetic relationship between zircon and uranium minerals provides evidence for the age of crystallization and mineralization.
(1) Betafite Betafite is mainly hosted in the intergranular fissures of rock-forming minerals in the U-rich granitic pegmatite (Figure 5a,b). The aggregation of betafites was also observed in the U-rich granitic pegmatite (Figure 5c,d). In addition, the filling of quartz, K-feldspar, and other minerals can also be observed in the holes in the betafite (Figure 5d). These

Characteristics of Principal Uranium Minerals and Zircon
Scanning electron microscopy (SEM) showed that the main uranium minerals in the U-rich granitic pegmatite are betafite and uraninite. The paragenetic relationship between zircon and uranium minerals provides evidence for the age of crystallization and mineralization.
(1) Betafite Betafite is mainly hosted in the intergranular fissures of rock-forming minerals in the U-rich granitic pegmatite (Figure 5a,b). The aggregation of betafites was also observed in the U-rich granitic pegmatite (Figure 5c,d). In addition, the filling of quartz, K-feldspar, and other minerals can also be observed in the holes in the betafite (Figure 5d). These characteristics reveal that betafites and rock-forming minerals were formed during the crystallization process at the same stage. Ideally, betafite is an equiaxed octahedral crystal. But in fact the crystal shape of betafite in the U-rich granitic pegmatite was incomplete, and the developed fractures often extended into rocks (Figure 5a,b). These characteristics indicate that the U-rich granitic pegmatite veins may have been affected by later tectonism, which often destroyed the crystal shape of the betafite. were probably formed by the recrystallisation of elemental U from the previously formedbetafite.
(3) Zircon The genetic type of zircons and the paragenetic relationship between zircons and ore minerals are important bases for determining the age of crystallization and mineralization. Zircons with a prismatic shape and idiomorphic or subhedral crystal form can be observed under a scanning electron microscope (Figure 5e,f), which shows the same characteristics as zircon in the cathodoluminescence (CL) images. All these show the characteristics of magmatic zircons. Zircons occurred in the intergranular fissures of K-feldspar and were associated with uraninite ( Figure 5f). The above occurrence characteristics of zircons indicate mineralization of the U-rich granitic pegmatite during crystallization. Therefore, the zircon age can provide supporting chronological evidence for crystallization and mineralization.  Uraninite in the U-rich granitic pegmatite is associated with betafite, which indicates that it is closely related to genesis. Under a scanning electron microscope, it can be seen that there are two types of genesis of uraninite: uraninites were wrapped in betafite (Figure 5a), and other uraninites existed on the outer edge ( Figure 5b) or internal fissure of the betafite (Figure 5c). Because the crystallization temperature of uraninite is higher than that of betafite, the formation of uraninite wrapped in betafite may have occurred earlier than that of betafite during the magmatic crystallization of U-rich granitic pegmatites. The uraninite grains that grew in the internal fissures of betafite or on the outer edge of betafite were probably formed by the recrystallisation of elemental U from the previously formedbetafite.
(3) Zircon The genetic type of zircons and the paragenetic relationship between zircons and ore minerals are important bases for determining the age of crystallization and mineralization. Zircons with a prismatic shape and idiomorphic or subhedral crystal form can be observed under a scanning electron microscope (Figure 5e,f), which shows the same characteristics as zircon in the cathodoluminescence (CL) images. All these show the characteristics of magmatic zircons. Zircons occurred in the intergranular fissures of K-feldspar and were associated with uraninite ( Figure 5f). The above occurrence characteristics of zircons indicate mineralization of the U-rich granitic pegmatite during crystallization. Therefore, the zircon age can provide supporting chronological evidence for crystallization and mineralization.

Zircon U-Pb Geochronology
Older zircons (>1000 Ma) usually exhibit Pb loss. Under the same initial conditions and geological environment, 206 Pb and 207 Pb isotopes have synchronous variation characteristics and can maintain a relatively stable ratio [23]. Therefore, the 206 Pb/ 238 U age was used for zircons younger than 1000 Ma, and the 206 Pb/ 207 Pb age was used for zircons older than 1000 Ma to represent the formation age of zircons. Two groups representative of U-rich granitic pegmatite samples from the western Huayangchuan deposit were dated to determine their crystallization and mineralization epoch. Most zircons from the samples were translucent-transparent crystals. They had a size range of 150-300 µm long and 100-200 µm wide, with length:width ratios of 2:1-3:1. The CL images of the zircon grains ( Figure 6a) displayed clear concentric oscillatory zoning coupled with high Th:U ratios (most were 0.11-0.89, average = 0.56) (Tables 1 and 2), suggesting a magmatic origin [24]. Meanwhile, the chondrite-normalized REE patterns of the zircons were similar to those of typical magmatic zircons (Figure 7a Figure 8d), respectively. This age was interpreted as the crystallization age of the U-rich granitic pegmatite.

Major Elements
The major and trace element test data are presented in Tables 3 and 4. Most of the Urich granitic pegmatite samples from the Huayangchuan deposit had low LOI values, indicating that these samples were relatively fresh.

Major Elements
The major and trace element test data are presented in Tables 3 and 4 Figure 9d), respectively. In addition, it can also be seen that the U-rich granite pegmatite samples have different major element characteristics with the Paleoproterozoic Yuantou granite [27], Huashan granite, and TTG gneiss of the Taihua group (Figure 9a-d).

Trace Elements
The contents of rare earth elements (ΣREE) in the U-rich granitic pegmatite samples range from 430.50 to 1286.18 × 10 −6 ( Table 3), indicating that the REE in the U-rich granitic pegmatite had the characteristics of high total amount but very uneven distribution. In the chondrite-normalized diagrams (Figure 10a (Figure 10a). Moreover, all of the U-rich granitic pegmatite samples enriched in large-ion lithophile elements (such as Rb, Ba, K, and Pb) and radioactive elements (such as Th and U) and depleted in high-field-strength elements (such as Ta, P, Ti, Zr, and Hf) (Figure 10b). Obviously, the combination and enrichment characteristics of the trace elements in the U-rich granitic pegmatite samples were also consistent with the actual oreforming elements (such as U, Pb, and REE). Compared with the Yuantou granite [27], Huashan granite, and the TTG gneiss of the Taihua group, the U-rich granite pegmatite sample has a higher total amount of rare earth elements (Figure 10a), as well as Th, U, Pb, and other trace element combinations (Figure 10b). This characteristic is also consistent with the actual metallogenic element combinations (such as U, Pb, REE, etc.) in this area.

Trace Elements
The contents of rare earth elements (ΣREE) in the U-rich granitic pegmatite samples range from 430.50 to 1286.18 × 10 −6 ( Table 3), indicating that the REE in the U-rich granitic pegmatite had the characteristics of high total amount but very uneven distribution. In the chondrite-normalized diagrams (Figure 10a (Figure 10a). Moreover, all of the U-rich granitic pegmatite samples enriched in large-ion lithophile elements (such as Rb, Ba, K, and Pb) and radioactive elements (such as Th and U) and depleted in high-field-strength elements (such as Ta, P, Ti, Zr, and Hf) (Figure 10b). Obviously, the combination and enrichment characteristics of the trace elements in the U-rich granitic pegmatite samples were also consistent with the actual ore-forming elements (such as U, Pb, and REE). Compared with the Yuantou granite [27], Huashan granite, and the TTG gneiss of the Taihua group, the U-rich granite pegmatite sample has a higher total amount of rare earth elements (Figure 10a), as well as Th, U, Pb, and other trace element combinations (Figure 10b). This characteristic is also consistent with the actual metallogenic element combinations (such as U, Pb, REE, etc.) in this area.
( Figure 10b). Obviously, the combination and enrichment characteristics of the trace elements in the U-rich granitic pegmatite samples were also consistent with the actual oreforming elements (such as U, Pb, and REE). Compared with the Yuantou granite [27], Huashan granite, and the TTG gneiss of the Taihua group, the U-rich granite pegmatite sample has a higher total amount of rare earth elements (Figure 10a), as well as Th, U, Pb, and other trace element combinations (Figure 10b). This characteristic is also consistent with the actual metallogenic element combinations (such as U, Pb, REE, etc.) in this area.

Zircon Lu-Hf Isotopic Analysis
Twenty zircon grains from the two groups of zircon samples were analyzed for their Hf isotopic compositions. The results of the Lu-Hf analysis are presented in Table 5 Figure 11a). Correspondingly, their single-(tDM1) and two-stage (tDM2) model ages ranged from 2.61 to 2.41 Ga and from 3.10 to 2.76 Ga (Table 5, Figure 11b), respectively. The Hf isotope composition of the zircon indicates that the Late Paleoproterozoic U-rich granitic pegmatite in Huayangchuan was probably formed by the reworking or remelting of crustal material from the Middle Archean to the Neoarchean.

Zircon Lu-Hf Isotopic Analysis
Twenty zircon grains from the two groups of zircon samples were analyzed for their Hf isotopic compositions. The results of the Lu-Hf analysis are presented in Table 5 Figure 11a). Correspondingly, their single-(t DM1 ) and two-stage (t DM2 ) model ages ranged from 2.61 to 2.41 Ga and from 3.10 to 2.76 Ga (Table 5, Figure 11b), respectively. The Hf isotope composition of the zircon indicates that the Late Paleoproterozoic U-rich granitic pegmatite in Huayangchuan was probably formed by the reworking or remelting of crustal material from the Middle Archean to the Neoarchean.

Constraints from Zircon Ages Paleoproterozoic U Mineralization
Based on field observations, the U-rich granitic pegmatite veins intruded into the Taihua group, and the intrusive boundary with the Taihua group was clearly visible (Figure 3a,b), indicating the characteristics of a magmatic intrusion. The CL images of zircons from U-rich granitic pegmatite samples also showed general characteristics of magmatic zircons [24]. The REE characteristics of the zircons were consistent with those of typical magmatic zircons (Figure 7a,c). The highly positive correlation of U and Th in zircon

Constraints from Zircon Ages Paleoproterozoic U Mineralization
Based on field observations, the U-rich granitic pegmatite veins intruded into the Taihua group, and the intrusive boundary with the Taihua group was clearly visible (Figure 3a,b), indicating the characteristics of a magmatic intrusion. The CL images of zircons from U-rich granitic pegmatite samples also showed general characteristics of magmatic zircons [24]. The REE characteristics of the zircons were consistent with those of typical magmatic zircons (Figure 7a,c). The highly positive correlation of U and Th in zircon showed the characteristics of magmatic genesis (Figure 7b,d), reflecting that the zircon isotope system was still well sealed without the migration of U and Th. Under the polarizing and scanning electron microscopes, zircon grains displayed an intact crystal shape (Figures 3c and 5e,f) and an association with uraninite (Figure 5f). Combined with the betafites in the intergranular fissures of rock-forming minerals (Figure 5a-d), we speculate that the zircons had mineralization characteristics in the crystallization stage. Therefore, the zircon U-Pb dating results obtained in this study were 1826.3 ± 7.9 and 1829 ± 11 Ma (Figure 8b,d), which not only indicated the crystallization age of U-rich pegmatite but also represented the age of uranium mineralization in the same period.
Generally, orogenic belts on the margins of ancient continental blocks are important uranium metallogenic regions. First, ancient land blocks are often rich in large-ion lithophilic elements (e.g., Rb, Ba, Th, U, and K), which can easily provide material sources for uranium polymetallic mineralization. Second, the crust and mantle materials on the margin of the ancient continental region have strong material interactions and frequent magmatic activities, which can create favorable geological conditions for the large-scale enrichment of ore-forming materials. Therefore, the marginal zone of the ancient continent often had favorable uranium polymetallic mineralization conditions that controlled the temporal and spatial distribution of uranium polymetallic deposits [30,31]. Regionally, a large number of late Paleoproterozoic (2.0-1.8 Ga) uranium polymetallic deposits are distributed along the collisional orogenic belt along the marginal zone of the ancient continental North China Craton. Typical deposits include the Lianshanguan uranium deposit in Liaoning Province, the Pinglu uranium deposit in Shanxi Province, and the Hongshiquan uranium deposit in Gansu Province [30,31]. In conclusion, the chronological research results of U-rich granitic pegmatite in this study show that uranium mineralization in the late Paleoproterozoic (1829 ± 11 and 1826 ± 7.9 Ma) also occurred in the Xiaoqinling area of the southern margin of the North China Craton, which implies that the tectonicmagmatic-mineralization events were produced during the ultimate cratonization process of the North China Craton in the late Paleoproterozoic (2.0-1.8 Ga) [32][33][34].

Rock Type of the U-Rich Granitic Pegmatite
Lithologically, A-type granites can be further divided into peralkaline and aluminous types [35]. Peralkaline A-type granite with a high degree of magmatic differentiation is generally formed during the latest time series of magmatic activity. They are often associated with mafic rocks (such as mafic inclusions, xenoliths, and intrusive veins) and often contain alkaline dark minerals (such as aegirine, aegirine-augite, sodium amphibole, sodium iron amphibole, and olivine) [36]. The peralkaline A-type granite is characterized by high SiO 2 , rich total alkalis (K 2 O + Na 2 O), and relatively poor MgO and low CaO; they usually enriched large-ion lithophile elements (LILEs: such as Rb, Th, U, and K) and depleted high-field-strength elements (HFSEs: such as Zr, Ta, and Ti) [37]. Their ΣREEs are usually several times or even dozens of times greater than that of other types of granites, and they have strong negative δEu anomalies in the chondrite-normalized diagrams [38]. They usually also have high K 2 O/Na 2 O values, A/CNK ratios >1, and 10,000 × Ga/Al ratios > 2.6. Compared to peralkaline A-type granites, aluminous Atype granites have a relatively low degree of magmatic differentiation [39]; therefore, they also show slightly different mineral and geochemical characteristics. The aluminous A-type granite is relatively rich in aluminum (Al 2 O 3 > 12 wt.%), but the A/CNK and 10,000 × Ga/Al value are relatively low. They have a high content of light REE, thus showing more obvious characteristics of light and heavy rare earth fractionation, but δEu is usually not obvious [38]. The dark minerals of aluminous A-type granites are mainly ordinary hornblende or biotite [40].
The U-rich granitic pegmatite samples in this study were characterized by high  (Figure 12d), which also shows different rock type characteristics from the Huashan granite and TTG of the Taihua group. The trace elements of the U-rich granitic pegmatite samples also showed enrichment of large-ion lithophile elements (typically Rb, Ba, K, and Pb) and radioactive elements (such as Th and U) and depletion of high-field-strength elements (such as Ta, P, Ti, and Hf ( Figure 10b). The U-rich granitic pegmatite samples also have a high total content of rare earth elements (ΣREE), but fractionation characteristics of LREE and HREE are obvious, and negative δEu anomalies are relatively weak (Figure 10a). Alkaline dark minerals (such as aegirine, aegirine-augite, sodium amphibole, sodium iron amphibole, and olivine) were not found in the U-rich granitic pegmatite samples ( Figure 4). In summary, the U-rich granitic pegmatites of the late Paleoproterozoic in the Huayangchuan deposit were equivalent to aluminous A-type granites.
Ti, and Hf (Figure 10b). The U-rich granitic pegmatite samples also have a high total content of rare earth elements (ΣREE), but fractionation characteristics of LREE and HREE are obvious, and negative δEu anomalies are relatively weak (Figure 10a). Alkaline dark minerals (such as aegirine, aegirine-augite, sodium amphibole, sodium iron amphibole, and olivine) were not found in the U-rich granitic pegmatite samples (Figure 4). In summary, the U-rich granitic pegmatites of the late Paleoproterozoic in the Huayangchuan deposit were equivalent to aluminous A-type granites.

Tectonic Setting of U Mineralization
Type A granites are generally formed in tensile or extensional tectonic settings [36]. Tectonic settings can be divided into non-orogenic and post-orogenic types [41]. Globally, A-type granites were very rare before the Paleoproterozoic but began to appear in large quantities during the late Paleoproterozoic (early Mesoproterozoic) [42]. This phenomenon implies a transition of the tectonic system from compression to extension during the continental evolution [43]. During the late Paleoproterozoic (2.0-1.8 Ga), all kinds of rocks in the basement of the North China Craton underwent strong metamorphism and deformation [44]. This process lasted at least 150 Ma, which included widespread land-land collision events, and this tectonic event was known as the Luliang movement [45]. The Luliang movement promoted a unified crystalline basement in the North China Craton. A series of magmatic activities occurred in the North China Craton after the Luliang movement. For example, Yang (2020) [46] obtained zircon U-Pb ages of felsic pegmatite, granodiorite, and monzogranite in the Xiaoqinling area on the southern margin of the North China Craton, which were aged approximately 1926, 1808, and 1807 Ma, respectively, reflecting tectonic magmatism after the end of the Luliang movement. Thereafter, the bimodal volcanic rocks of the Xiong'er group (1.80-1.75 Ga) [47], the volcanic-sedimentary formation of the Changcheng group (1.68-1.62 Ga) [48], and the contemporaneous or later (1.72-1.60 Ga) basic dyke swarms [49] all indicate that the Xiaoqinling area on the southern margin of the North China Craton had been in a continuous regional extensional environment since the Luliang movement.
In the SiO 2 vs. lg[Ca/(Na 2 O + K 2 O)] diagram ( Figure 13a) and R 1 vs. R 2 diagram (Figure 13b), most of the U-rich granitic pegmatite samples were plotted in an extensional and non-orogenic tectonic setting. In the Y vs. Nb diagram (Figure 14a), Yb vs. Ta diagram (Figure 14b), Y + Nb vs. Rb diagram (Figure 14c), and Yb + Ta vs. Rb diagram (Figure 14d), most of the U-rich granitic pegmatite samples are generally in an intra-plate granite tectonic setting (WPG) [50]. In the Y-Nb-3×Ga diagram (Figure 15a), Y-Nb-3×Ce diagram (Figure 15b), and Yb + Ta vs. Rb diagram (Figure 15d), most of the U-rich granitic pegmatite samples belong to intraplate A 1 -type granite [36]. Therefore, the above results indicate that the Xiaoqinling belt in the southern margin of the North China Craton was already in a non-orogenic extensional setting when the U-rich granitic pegmatites were formed (1826.3 ± 7.9 and 1829 ± 11 Ma). The reconstruction scheme of the Columbia supercontinent in the late Paleoproterozoic (2.0-1.8 Ga) provided the location of the North China Craton. At this time, the southern margin of the North China Craton was located in the intraplate rift zone of the Columbian supercontinent [51], which had the non-orogenic tectonic conditions of a plate margin or intraplate rift.
Type A granites are generally formed in tensile or extensional tectonic settings [36]. Tectonic settings can be divided into non-orogenic and post-orogenic types [41]. Globally, A-type granites were very rare before the Paleoproterozoic but began to appear in large quantities during the late Paleoproterozoic (early Mesoproterozoic) [42]. This phenomenon implies a transition of the tectonic system from compression to extension during the continental evolution [43]. During the late Paleoproterozoic (2.0-1.8 Ga), all kinds of rocks in the basement of the North China Craton underwent strong metamorphism and deformation [44]. This process lasted at least 150 Ma, which included widespread land-land collision events, and this tectonic event was known as the Luliang movement [45]. The Luliang movement promoted a unified crystalline basement in the North China Craton. A series of magmatic activities occurred in the North China Craton after the Luliang movement. For example, Yang (2020) [46] obtained zircon U-Pb ages of felsic pegmatite, granodiorite, and monzogranite in the Xiaoqinling area on the southern margin of the North China Craton, which were aged approximately 1926, 1808, and 1807 Ma, respectively, reflecting tectonic magmatism after the end of the Luliang movement. Thereafter, the bimodal volcanic rocks of the Xiong'er group (1.80-1.75 Ga) [47], the volcanic-sedimentary formation of the Changcheng group (1.68-1.62 Ga) [48], and the contemporaneous or later (1.72-1.60 Ga) basic dyke swarms [49] all indicate that the Xiaoqinling area on the southern margin of the North China Craton had been in a continuous regional extensional environment since the Luliang movement.
In the SiO2 vs. lg[Ca/(Na2O + K2O)] diagram ( Figure 13a) and R1 vs. R2 diagram (Figure 13b), most of the U-rich granitic pegmatite samples were plotted in an extensional and non-orogenic tectonic setting. In the Y vs. Nb diagram (Figure 14a), Yb vs. Ta diagram (Figure 14b), Y + Nb vs. Rb diagram (Figure 14c), and Yb + Ta vs. Rb diagram (Figure 14d), most of the U-rich granitic pegmatite samples are generally in an intra-plate granite tectonic setting (WPG) [50]. In the Y-Nb-3×Ga diagram (Figure 15a), Y-Nb-3×Ce diagram (Figure 15b), and Yb + Ta vs. Rb diagram (Figure 15d), most of the U-rich granitic pegmatite samples belong to intraplate A1-type granite [36]. Therefore, the above results indicate that the Xiaoqinling belt in the southern margin of the North China Craton was already in a non-orogenic extensional setting when the U-rich granitic pegmatites were formed (1826.3 ± 7.9 and 1829 ± 11 Ma). The reconstruction scheme of the Columbia supercontinent in the late Paleoproterozoic (2.0-1.8 Ga) provided the location of the North China Craton. At this time, the southern margin of the North China Craton was located in the intraplate rift zone of the Columbian supercontinent [51], which had the non-orogenic tectonic conditions of a plate margin or intraplate rift.

Metallogenic Models of the U-Rich Granitic Pegmatite
Currently, there are four viewpoints on the genetic model of A-type granite: first, the crustal rocks are partially melted to form I-type granite, and then the residual materials are partially melted again to form A-type granite [54]. However, experimental petrology and actual observations proved that the residual crustal material cannot differentiate A-type granite [55]. Second, A-type granite is formed by the partial melting of the crystalline basement or metamorphic sedimentary rocks [35]. Third, A-type granite is formed by crustmantle magmatic mixing [56]. Fourth, the separation crystallization of mantle-derived alkaline basalt directly forms A-type granite [57]. The studied U-rich granitic pegmatite samples have the characteristics of high SiO 2 , Al 2 O 3 , and total alkalis, low MgO, TiO 2 , and P 2 O 5 , and enrichment in large-ion lithophiles and radioactive elements (such as Rb, Ba, Th, U, K, and Pb) and depletion of high-field-strength elements (such as Ta, P, Ti, and Hf). These whole-rock geochemical characteristics support the conclusion that the magma source of the U-rich granitic pegmatite samples was felsic crustal material, rather than mantle-derived mafic magma. In addition, experimental petrology has proved that felsic rocks in the shallow crust (depth ≤ 20 km) can produce A-type granites melted through dehydration, high temperature, and partial melting [58]. In fact, the lithology of the Taihua group as the basement was composed of "supracrustal rock" and "TTG suite" (Trondhjemite, Tonalite, and Granodiorite), whose material composition clearly belongs to the evolved felsic crust. The formation ages of Taihua group were approximately 2.8, 2.5, 2.3, and 1.97-1.80 Ga [32,34,59], reflecting the multi-stage cyclic evolution of the crust in this area. The formation age of the early Taihua group (approximately 2.8 Ga) is much older than that of the later U-rich granitic pegmatite and is very close to the two-stage model age (T DM2 ) of the zircon Hf isotope (3.10-2.76 Ga). This evidence indicates that the materials of the early Taihua group (such as the Middle Archean) were probably the magma source of the later Taihua group (such as the Late Paleoproterozoic).
Therefore, we can speculate that the formation process of U-rich granitic pegmatite in this study was as follows: after the Late Paleoproterozoic (1826.3 ± 7.9 and 1829 ± 11 Ma) Luliang movement, the tectonic setting in this area gradually transitioned to an extensional background [27]. The subduction plates broke off and triggered asthenospheric mantle upwelling, resulting in partial melting of the lithospheric mantle, and the generated basic magma rose and underplated the middle-lower crust, prompting partial melting of the early Taihua group formed in the Archean-Neoarchean (3.10-2.76 Ga). As extension continued, a series of A-type granites gradually formed, such as in the Yuantou and Huayangchuan areas (Figure 16a). The Taihua group formed in the Archean-Neoarchean period was rich in uranium and other radioactive elements, and the uranium-rich granitic pegmatites in this area were directly formed during the magmatic activity in the late Paleoproterozoic (1826.3 ± 7.9 and 1829 ± 11 Ma) (Figure 16b). These U-rich granitic pegmatites also provided material sources for later (Indosinian and Yanshanian) uranium mineralization in the Huayangchuan area or underwent superimposed transformation to form new deposit types, reflecting the ultra-long evolutionary history of uranium mineralization and uranium deposits with complex genesis in the Huayangchuan area.
ing of the early Taihua group formed in the Archean-Neoarchean (3.10-2.76 Ga). As extension continued, a series of A-type granites gradually formed, such as in the Yuantou and Huayangchuan areas (Figure 16a). The Taihua group formed in the Archean-Neoarchean period was rich in uranium and other radioactive elements, and the uranium-rich granitic pegmatites in this area were directly formed during the magmatic activity in the late Paleoproterozoic (1826.3 ± 7.9 and 1829 ± 11 Ma) (Figure 16b). These U-rich granitic pegmatites also provided material sources for later (Indosinian and Yanshanian) uranium mineralization in the Huayangchuan area or underwent superimposed transformation to form new deposit types, reflecting the ultra-long evolutionary history of uranium mineralization and uranium deposits with complex genesis in the Huayangchuan area.

Conclusions
(1) The U-rich granitic pegmatites were formed in the late Paleoproterozoic (1826.3 ± 7.9 and 1829 ± 11 Ma). The paragenetic phenomena of the magmatic zircons with betafite and uraninite in the samples showed metallogenic characteristics during the crystallization period.

Conclusions
(1) The U-rich granitic pegmatites were formed in the late Paleoproterozoic (1826.3 ± 7.9 and 1829 ± 11 Ma). The paragenetic phenomena of the magmatic zircons with betafite and uraninite in the samples showed metallogenic characteristics during the crystallization period. (2) Based on the classification criteria and rock characteristics of A-type granite, the major elements, trace elements, and mineral compositions of most U-rich granitic pegmatite samples had the characteristics of intraplate A 1 -type granite (3) The U-rich granitic pegmatites were formed after the Luliang movement in the late Paleoproterozoic, and the tectonic system gradually transitioned from a continentcontinent collision to an extensional setting. The partial melting of the early Taihua group materials formed in the Archean-Neoarchean period triggered a series of tectonic granitic magmatic activities. (4) The early Taihua group formed in the Archean-Neoarchean period as mature crust material rich in uranium, which provided uranium-rich magma for the formation of uranium-rich granite pegmatite in the late Paleoproterozoic. Existing uranium-rich geological bodies also provided material sources for later uranium mineralization in the Huayangchuan deposit.