Geophysical Parameter Response Characteristics of the Dagele Niobium Deposit in the Eastern Kunlun Region (China)

Abstract

Niobium is a strategic critical mineral that supports emerging energy and high-end manufacturing. The geophysical parameters of carbonatite-alkaline rock-type niobium deposits constitute essential baseline data for regional geophysical exploration and prospecting target delineation. To clarify the geophysical response characteristics and exploration the significance of the Dagele niobium deposit in the Eastern Kunlun Region (western China). This study focuses on drill hole ZK3202. Samples from ore bodies, mineralized zones, and wall rocks of different lithologies were continuously measured. Combined with 1001.8 m of full-hole core digital logging data, statistical methods, including box plots, histograms, multi-parameter cross-plots, and correlation coefficient analysis, were applied to quantitatively investigate the physical property responses of lithologies such as calcite-biotite rock (ore body), calcite-bearing pyroxenite (mineralized zone) and amphibolite in the vertical profile. Lithological identification thresholds were established to divide the drill-hole into lithological and mineralized ore layers. The results show that the ore-bearing lithofacies exhibit a distinctive geophysical signature characterized by high density, strong magnetism, medium-low resistivity, high polarizability, and slightly elevated natural radioactivity, which clearly distinguishes them from surrounding from wall rocks. Based on five key parameters—density, magnetic susceptibility, resistivity, polarizability, and natural gamma—a lithological identification model for amphibolite and mineralized altered rock assemblages was established. This study also summarizes the multi-parameter coupling mechanism of ore-bearing lithofacies, which can effectively delineate favorable niobium-bearing horizons. This work fills a gap in the geophysical property characterization of carbonatite-alkaline complex-type niobium deposits in the Eastern Kunlun region and provides data support and regional reference for integrated gravity-magnetic-electrical-radioactive geophysical exploration, prospecting target delineation, and the exploration of similar niobium deposits in western China.

1. Introduction

Niobium is a strategic critical mineral, widely used in superconducting materials, high-grade alloy steels, semiconductor devices, and other advanced technologies [1]. Its exploration has therefore become an important component of China’s mineral resource security. Carbonatite-alkaline complexes represent the main metallogenic type of niobium deposits worldwide [2,3]. The geophysical parameters of these complexes provide essential baseline data for improving the efficiency of geophysical exploration efficiency and for establishing reliable prospecting models [4].

The Eastern Kunlun orogenic belt is an important polymetallic metallogenic belt in western China (Figure 1a). The recently discovered Dagele niobium deposit, a carbonatite-alkaline complex-type deposit in this region, fills a long-standing regional gap in carbonatite-hosted niobium mineralization, previously noted by [5,6,7], and exhibits significant exploration potential and scientific value. However, existing studies have mainly focused on geological genesis and metallogenic processes, while systematic measurements and analyses of geophysical parameters remain limited, resulting in insufficient baseline data to support regional geophysical exploration [8]. Moreover, the Eastern Kunlun region is characterized by complex geological structures, frequent magmatic activity, and diverse wall-rock lithologies. The often subtle physical property contrasts between rocks and ores further complicate exploration and constitute a major constraint on niobium prospecting in this area [9].

In this context, the Dagele niobium deposit is selected as the focus of this study. Based on geophysical measurements of ore-bearing lithofacies, mineralized zones, and surrounding wall rocks, key physical parameters, including density, magnetic and electrical properties, and radioactivity are systematically characterized. Their response patterns and contrasts are analyzed, and their implications for exploration are discussed. A multi-parameter lithological response framework is established, leading to the development of a lithological identification model and a synthesis of the coupling mechanisms of ore-bearing lithofacies.

The results aim to fill the gap in geophysical property studies of the Dagele niobium deposit, provide data support for integrated regional geophysical exploration, and enrich the physical property database of alkaline rock-type niobium deposits in western China [10]. This work defines clear research objectives and emphasizes its scientific novelty through the development of a multi-parameter geophysical prospecting model for carbonatite-alkaline niobium deposits. Such integrated, multidisciplinary geophysical frameworks are widely applied in major metallogenic belts worldwide, and the methodology adopted here aligns with current trends in international geophysics exploration.

2. Geological Setting

2.1. Geological Characteristics

Dagele is located in the northeastern Qinghai-Tibet Plateau and tectonically belongs to the North Kunlun magmatic arc of the Eastern Kunlun Orogenic Belt (Figure 1b), situated between the Middle Kunlun Fault Zone (F2) and the South Kunlun Fault Zone (F3) [11]. The regional tectonic framework is dominated by NWW- and NW-trending compressional and transpressional faults, which serve as both ore-controlling and ore-conducting structures [11]. Stratigraphic units from the Lower-Middle Proterozoic to the Jurassic are exposed in the region. Among them, the Lower-Middle Proterozoic felsic gneiss forms the metamorphic basement and is closely related to mineralization. Magmatic rocks form a large petrographic belt dominated by granites, with minor mafic-ultramafic rocks, emplaced from the Proterozoic to the Late Mesozoic; the principal rock types are Silurian-Devonian and Permian-Triassic granites. The carbonatite-alkaline complexes associated with niobium mineralization were emplaced at 418–382 Ma [12]. The Eastern Kunlun Orogenic Belt is an important enrichment zone for strategic minerals in China, where several large to super-large deposits, such as the Baiganhu W-Sn deposit and the Xarihamu Ni deposit, have been discovered in the surrounding areas.

The strata exposed in the Dagele niobium ore district are dominated by the Lower Proterozoic Jinshuikou Group (Figure 1c), an amphibolite-facies metamorphic assemblage composed mainly of gneiss, schist and marble [13]. These rocks constitute the main body of the study area and the wall rocks of the ore-bearing complex. Locally developed strong phlogopitization alteration zones are closely associated with niobium mineralization and can serve as prospecting indicators. Tectonic activity in the district is intense, with three sets of faults (NW-, NE- and nearly NS-trending) that provide pathways and space for magmatic activity and ore-fluid migration, thereby controlling the formation and distribution of niobium orebodies. The ore-bearing complex displays a zonal lithological distribution from margin to center: amphibolite → olivine pyroxenite (calcite-bearing pyroxenite) → calcite mica rock → carbonatite [14]. Olivine pyroxenite constitutes the main niobium-bearing mineralized lithofacies, whereas calcite mica rock and carbonatite host the most intensive niobium mineralization; overall, the complex exhibits pervasive niobium mineralization. Niobium in carbonatite is mainly hosted by columbite group minerals niocalite and pyrochlore. Columbite group minerals commonly occur with loparite, magnetite and apatite, typically as fine-grained aggregates replacing magnetite along fractures and margins. Niocalite and pyrochlore are associated with columbite-group minerals, magnetite, and apatite and locally occur along grain boundaries, intragranular cavities, or fractures of magnetite. Pyrrhotite commonly replaces magnetite and is subsequently altered by limonite [15,16]. A total of five niobium orebodies have been delineated in the district (including the concealed orebody M5). Their strike lengths range from 160 to 1280 m, thicknesses from 4.3 to 115.7 m, and average Nb₂O₅ grades from 0.092% to 0.156%. The inferred Nb₂O₅ resource exceeds 200,000 tons. The orebodies extend continuously along the strike and dip, indicating significant exploration potential.

2.2. Drill Hole Information and Physical Property Testing Methods

In this study, drill hole ZK3202, located in the southeastern part of the Dagele niobium ore district, was selected as the research object. The borehole intersects two niobium orebodies (M2 and M5) and has a final depth of 1001.8 m, with a dip angle of 90°, an azimuth of 30°, an opening diameter of 108 mm, and a final diameter of 75 mm. The main lithologies encountered include amphibolite, diorite porphyrite, calcite mica rock, calcite-bearing pyroxenite, diabase, aegirine syenite, and granitic gneiss. Wall-rock alteration is dominated by phlogopitization, aegirine syenitization, and carbonatization, with minor pyritization and magnetitization, mainly developed in the hanging wall.

Core samples were systematically collected from the collar to the bottom of the borehole, according to lithology, during drilling in 2025. The sampling interval ranges from 2.16 to 1001.6 m, yielding a total of 618 samples, which cover both the ore bearing complex and surrounding wall rocks and use the principles of representativeness and systematic sampling [17,18]. The physical property measurements were conducted as follows: (i) Density: The measurements were performed on 416 samples under fully saturated conditions using the water-displacement method with a high-precision electronic balance (Longbei Precision Electronic Weighing Instrument, Yongkang, China). The measurements followed standard laboratory procedures for the density determination of rock samples. (ii) Magnetic properties: Magnetic susceptibility was measured on 416 samples using an SM-30 magnetic susceptibility meter (origin: ZH Instruments, Brno, Czech Republic, sensitivity: 1 × 10⁻⁷ SI; operating frequency: 8 kHz). In addition, remanent magnetization was measured simultaneously in 202 samples using an ENVI PRO high-precision proton magnetometer (second Gaussian position; origin: Scintrex Ltd., Concord, ON, Canada; absolute accuracy: ±1 nT; sensitivity: 0.1 nT) to determine both magnetic susceptibility and remanent magnetization simultaneously, allowing for comprehensive magnetic property characterization [19]. (iii) Electrical properties: The measurements were conducted on 618 samples using a WDJD-4 multi-function digital DC IP instrument (origin: Chongqing Pentium Numerical Control Technology Research Institute, Chongqing, China; 24-bit A/D converter; voltage and current accuracy: ±0.4% ±1 LSB) with the four-electrode method (power supply time 12 s, turn-off delay 200 ms, 3 stackings) to improve signal quality and reduce measurement noise [20]. Samples were soaked in clean water for 24 h and air-dried for 1 h before measurement using the saturated copper sulfate paste method to ensure good electrode contact. (iv) Gamma-ray spectrometry: The measurements were conducted on 416 samples using an ARD handheld multi-channel γ spectrometer (origin: Hebei Hangyao Technology Co., Ltd., Shijiazhuang, China, equipped with a 75 × 75 mm NaI(Tl) detector, energy resolution: ≤7.5% @ 662 keV), with a counting time of 30 s and 4 stackings per sample, to obtain reliable values for ²³⁸U, ²³²Th, ⁴⁰K, and total radioactivity [21].

2.3. Rock Types and Mineral Composition Analysis of Samples

The samples were classified into three categories: complex rocks, intrusive dikes, and wall rocks. Their mineral compositions reflect multi-stage geological processes and exhibit significant spatial and temporal variations [22]. The complex rocks constitute the main lithology of the metallogenic belt and occur as small stock groups in the eastern Dashuigou area, forming in a ring shape distribution. The complex intrudes mainly into the gneiss of the Jinshuikou Group, while its northern part is intruded by Early Devonian granodiorite (Figure 2).

Due to hydrothermal alteration and tectonic activity, the boundaries of the complex are irregular and locally indistinct. The complex comprises a heterogeneous assemblage of alkaline rock series, derived from mantle magma at different evolutionary stages [23]. The early stage is represented by barren mafic rocks (amphibolite and gabbro), whereas the late stage includes ore-bearing, magnetically enhanced ultrabasic rocks such as calcite-biotite rock, olivine pyroxenite, and igneous carbonatite. The core is dominated by calcite-biotite rock and dolomitic carbonatite, which intrude on the surrounding pyroxenite as layered and vein-like bodies. These lithologies commonly exhibit pervasive niobium and phosphorus mineralization and relatively strong magnetism. Calcite-biotite rock is the principal ore-bearing lithofacies, followed by pyroxenite and dolomitic carbonatite. The outer shell and upper part consist mainly of amphibolite, with minor gabbro, and are generally weakly magnetic. Mineralization is controlled by fractional crystallization, with the highest enrichment occurring in late-stage carbonatite. In apatite-bearing calcite-biotite rock, metallic minerals include ~3% subhedral granular titanomagnetite and ~1% disseminated anhedral pyrrhotite, commonly in contact with titanomagnetite. Apatite-bearing phlogopite-nepheline clinopyroxenite contains ~3% pyrrhotite, ~1% limonite, and minor chalcopyrite. Pyrrhotite typically occurs as subhedral grains, locally altered to pyrite and limonite along grain margins, whereas chalcopyrite forms irregular grains partly replaced by limonite. Amphibolite shows a clear intrusive contact with the gneiss of the Jinshuikou Group and is interpreted as metamorphosed gabbro. Its metallic minerals comprise ~2% pyrite, ~1% pyrrhotite, and trace chalcopyrite and ilmenite. The carbonatite-alkaline complex is the sole ore-bearing body for niobium mineralization in the area. Its complex mineral assemblages reflect prolonged, multi-stage mantle-derived magmatism, resulting in strong heterogeneity in rock physical properties [24].

Intrusive dikes are widespread and lithologically diverse. They are closely related to multi-stage magmatic activity and are structurally controlled, typically occurring along joints and bedding planes. The main types include alkaline, mafic, and intermediate dikes. Alkaline dikes are mainly represented by aegirine syenite, composed predominantly of nepheline and aegirine (or aegirine-augite), and occur discontinuously as bands and veins. Aegirine syenitization is the most common alkali metasomatic alteration in the hanging wall of the calcite-biotite niobium orebody. It reflects alkali-rich fluids exsolved from carbonatite magma and thus serves as an important indicator of deep concealed orebodies. Mafic dikes are dominated by diabase, which occurs in variable sizes and typically forms as nearly vertical. They are mainly composed of plagioclase, pyroxene, metallic minerals, apatite, and tourmaline. Intermediate dikes are represented by diorite porphyry, emplaced along bedding, schistosity (gneissosity), and joints. They display a porphyritic texture, with plagioclase and hornblende as the main phenocrysts.

Wall rocks are dominated by gneisses of the Jinshuikou Group, mainly biotite-plagioclase gneiss and biotite monzonitic gneiss, whereas the drill hole intersects only granitic gneiss. Metamorphic minerals include sillimanite, almandine, cordierite, andalusite, biotite, and hornblende, with minor K-feldspar and andesine. Variations in mineral composition among these rock types, combined with magmatic-hydrothermal activity and tectonic deformation, collectively result in significant heterogeneity in rock physical parameters in the Dagele area. The coupling between these properties and geological processes provide diagnostic information for deep resource exploration and offer key constraints for interpretating exploration data [25,26].

3. Results and Analysis

The Dagele area has undergone multi-stage magmatic–hydrothermal–tectonic superimposed mineralization, resulting in complex physical properties and pronounced spatial variability [27]. Based on the physical property dataset from drill cores, this study conducts a lithology-specific, multi-parameter collaborative analysis and summarizes the response characteristics of rock density, magnetic, electrical, and radioactive parameters (

Table 1. Statistics of physical properties of main lithologies in hole ZK3202.

Parameter	Lithology	N	Main Range	Mean	Mean 95% CI	Median	Median 95% CI	Std. Dev.	Std. Dev. 95% CI	IQR	IQR 95% CI
Density (g/cm3)	calcite-biotite rock	105	2.46~3.94	3.16	3.08~3.23	3.07	3.02~3.14	0.37	0.32~0.41	0.42	0.28~0.69
	calcite-bearing pyroxenite	146	2.23~3.62	3.03	2.98~3.08	3.01	2.95~3.07	0.28	0.24~0.31	0.36	0.29~0.43
	amphibolite	79	2.34~3.74	3.08	3.01~3.15	3.06	3.02~3.09	0.31	0.24~0.35	0.36	0.24~0.43
	aegirine syenite	25	2.37~3.36	2.85	2.74~2.94	2.81	2.75~2.90	0.25	0.17~0.30	0.23	0.11~0.52
	diabase	25	2.40~3.54	2.99	2.86~3.12	2.92	2.72~3.30	0.35	0.27~0.40	0.61	0.30~0.74
	diorite porphyrite	23	2.24~3.35	2.94	2.80~3.05	2.99	2.75~3.11	0.31	0.21~0.38	0.44	0.24~0.59
	granite gneiss	13	2.52~3.47	2.91	2.75~3.06	2.81	2.74~3.02	0.31	0.17~0.37	0.28	0.05~0.72
Magnetic susceptibility (10−6 SI)	calcite-biotite rock	128	131~37,767	10,479	7862~13,278	3255	1844~5896	15,750	11,421~19,795	12,560	7291~22,272
	calcite-bearing pyroxenite	206	16~6630	1766	1104~2566	471	421~648	5467	1829~8374	1012	719~1296
	amphibolite	150	44~3233	1165	1015~1339	846	676~996	1067	870~1245	1217	914~1569
	aegirine syenite	27	14~1521	343	203~507	197	137~297	410	193~543	317	132~747
	diabase	32	12~664	980	442~1732	368	333~404	2111	366~3376	142	64~1422
	diorite porphyrite	43	4~1376	456	330~603	313	256~349	452	249~643	240	113~614
	granite gneiss	32	3~1284	472	284~662	243	88~711	535	360~696	794	382~940
Remanent magnetization (10−3 A/m)	calcite-biotite rock	32	76~6199	3096	1048~6359	495	210~1936	8216	1369~13,320	2289	865~4212
	calcite-bearing pyroxenite	60	41~1086	451	293~657	207	173~294	726	265~1058	324	158~522
	amphibolite	71	27~1451	585	415~793	272	181~457	833	439~1207	549	415~1036
	diorite porphyrite	20	20~503	203	101~347	103	50~190	296	80~460	181	65~334
	granite gneiss	19	22~212	140	95~202	106	73~181	123	51~186	122	48~148
Resistivity (Ω·M)	calcite-biotite rock	128	36~3247	1668	1186~2230	721	575~876	3106	1358~4391	1291	948~2072
	calcite-bearing pyroxenite	206	67~4750	1974	1579~2446	1027	775~1236	3199	1966~4366	1599	1299~2099
	amphibolite	150	95~4252	1549	1321~1821	987	859~1188	1575	1237~1887	1600	1053~2024
	aegirine syenite	27	49~2861	1439	869~2119	843	600~1483	1705	652~2550	1260	575~2205
	diabase	32	156~18,977	4749	2642~7366	1327	839~3851	6954	3693~9293	4476	1599~13,884
	diorite porphyrite	43	113~7747	2671	2050~3295	2039	1585~2770	2243	1526~2811	2640	1576~3831
	granite gneiss	32	32~5018	1239	697~1893	569	376~702	1849	884~2553	619	354~3353
Polarizability (%)	calcite-biotite rock	128	1~17	6.28	5.13~7.58	3.70	2.90~4.493	7.13	5.24~8.84	4.77	3.92~8.40
	calcite-bearing pyroxenite	206	0~8	4.03	3.20~4.93	1.87	1.70~2.225	6.38	4.34~8.11	2.58	1.98~3.43
	amphibolite	150	1~16	5.97	4.96~7.09	3.16	2.28~3.867	6.70	5.45~7.88	5.55	4.28~8.73
	aegirine syenite	27	0~3	2.74	1.05~5.60	1.04	0.82~1.397	6.62	0.69~10.79	1.02	0.49~2.38
	diabase	32	1~29	9.37	5.52~13.9	2.66	1.65~6.430	12.20	8.22~14.91	11.09	2.58~26.14
	diorite porphyrite	43	0~6	2.45	2.03~2.89	2.35	1.78~2.770	1.43	1.07~1.74	1.80	1.14~2.63
	granite gneiss	32	0~8	4.37	2.01~7.49	1.48	0.90~2.340	8.14	2.30~12.35	3.00	1.07~6.53
U content (10−6)	calcite-biotite rock	105	3.2~7.2	5.26	5.08~5.45	5.07	4.93~5.23	1.03	0.80~1.26	1.07	0.77~1.31
	calcite-bearing pyroxenite	146	3.0~6.6	4.85	4.73~4.96	4.78	4.64~4.99	0.71	0.63~0.78	1.05	0.89~1.24
	amphibolite	79	2.4~7.8	4.82	4.52~7.49	4.73	4.50~5.00	6.35	1.39~10.56	1.20	0.83~1.68
	aegirine syenite	25	3.7~5.7	4.78	4.58~4.96	4.90	4.52~5.07	0.49	0.36~0.59	0.60	0.38~0.99
	diabase	25	3.3~7.0	4.76	4.52~6.29	4.73	4.45~5.12	2.42	0.52~3.95	0.79	0.48~1.33
	diorite porphyrite	23	3.3~6.3	4.57	4.32~4.84	4.50	4.17~4.72	0.63	0.33~0.83	0.59	0.24~0.98
	granite gneiss	13	3.8~6.9	4.62	4.23~5.10	4.48	4.15~4.70	0.84	0.31~1.22	0.55	0.22~1.35
Th content (10−6)	calcite-biotite rock	105	10.7~15.6	13.15	12.93~13.35	13.20	12.93~13.43	1.11	0.88~1.32	1.66	1.32~1.98
	calcite-bearing pyroxenite	146	10.5~16.2	13.23	13.00~13.42	13.25	12.97~13.45	1.28	1.08~1.46	1.61	1.36~1.84
	amphibolite	79	11.0~17.5	13.73	13.39~14.05	13.50	13.22~13.95	1.50	1.19~1.79	2.00	1.60~2.40
	aegirine syenite	25	11.7~15.0	12.99	12.59~13.34	12.80	12.27~13.35	0.98	0.73~1.22	1.33	1.02~1.62
	diabase	25	12.0~15.0	13.17	12.63~13.58	13.40	12.90~13.72	1.25	0.99~1.49	1.10	0.88~1.32
	diorite porphyrite	23	11.3~15.8	13.48	13.08~13.83	13.60	13.17~13.90	0.95	0.71~1.18	0.84	0.67~1.00
	granite gneiss	13	11.0~15.2	13.35	12.75~13.86	13.60	12.82~14.00	1.06	0.79~1.33	1.18	0.94~1.41
K content (%)	calcite-biotite rock	105	0.87~1.58	1.22	1.18~1.24	1.23	1.16~1.27	0.15	0.13~0.17	0.23	0.19~0.26
	calcite-bearing pyroxenite	146	0.90~1.60	1.27	1.24~1.29	1.30	1.25~1.32	0.15	0.13~0.16	0.21	0.17~0.26
	amphibolite	79	0.87~1.43	1.22	1.19~1.24	1.23	1.20~1.25	0.12	0.10~0.14	0.14	0.10~0.18
	aegirine syenite	25	0.80~1.53	1.20	1.13~1.26	1.18	1.12~1.27	0.17	0.11~0.20	0.18	0.07~0.32
	diabase	25	0.90~1.48	1.17	1.11~1.22	1.18	1.06~1.27	0.14	0.10~0.16	0.21	0.10~0.28
	diorite porphyrite	23	1.10~1.55	1.28	1.23~1.33	1.28	1.20~1.32	0.12	0.08~0.15	0.16	0.10~0.25
	granite gneiss	13	1.25~1.53	1.39	1.33~1.43	1.38	1.32~1.45	0.09	0.05~0.10	0.13	0.02~0.20
Total radioactivity (API)	calcite-biotite rock	105	17.4~19.6	18.4	18.3~18.6	18.3	18.1~18.4	0.81	0.58~1.05	0.78	0.57~1.03
	calcite-bearing pyroxenite	146	17.1~19.1	18.0	17.8~18.0	18.0	17.8~18.0	0.58	0.37~0.84	0.56	0.40~0.65
	amphibolite	79	16.6~20.2	18.1	17.8~20.4	17.7	17.5~17.8	6.04	1.33~10.03	0.90	0.69~1.66
	aegirine syenite	25	16.8~18.8	17.6	17.3~17.7	17.6	17.2~17.8	0.51	0.36~0.63	0.65	0.42~0.99
	diabase	25	16.4~18.6	17.7	17.3~19.1	17.6	17.4~17.9	2.37	0.52~3.78	0.82	0.37~1.23
	diorite porphyrite	23	16.8~19.2	17.6	17.3~17.8	17.4	17.3~17.4	0.61	0.29~0.78	0.26	0.10~1.30
	granite gneiss	13	17.1~19.6	18.1	17.7~18.5	18.3	17.5~18.3	0.75	0.46~0.94	0.85	0.25~1.60

, Figure 3a).

3.1. Statistical Analysis of Physical Parameters Using Box Plots

Based on multi-parameter physical data from all drill cores, box plots combined with normal distribution curves were used to identify distribution patterns, anomalies, and statistical trends. This integrated approach helps clarify the geological controls on the observed properties. Density values (Figure 3b) range from 2.2 to 4.0 g/cm³, nearly doubling across the interval. High-density zones are concentrated in deep magnetite-pyrite association zones of the main orebody and in high-grade alkaline rock–carbonatite-type niobium orebodies. Low-density lithologies, such as granitic gneiss, aegirine syenite, and diorite porphyrite, form the regional background field. Pyrrhotite and ilmenite-bearing amphibolite, calcite-bearing pyroxenite, and some limonite-altered dikes also display relatively high densities, with the anomaly magnitude generally proportional to their scale.

Magnetic susceptibility values (Figure 3c) range from 0 to 40,000 × 10⁻⁶ SI, spanning four orders of magnitude. Magnetic properties are mainly controlled by the content, grain size, distribution, and oxidation state of ferromagnetic minerals, dominated by magnetite, followed by pyrrhotite and ilmenite. Magnetite susceptibility is positively correlated with an abundance of these minerals in ultramafic rocks. Magnetite is the primary factor responsible for high magnetic anomalies; strong magnetic responses are mainly associated with magnetite-rich orebodies and mineralized rocks, and susceptibility increases rapidly with increasing magnetite grade. Calcite-bearing pyroxenite and amphibolite exhibit moderate magnetic susceptibility, typically around 1000 × 10⁻⁶ SI, with some samples at 3000 × 10⁻⁶ SI. In contrast, unmineralized aegirine syenite, diabase, diorite porphyrite, and granitic gneiss display magnetic susceptibility values below 500 × 10⁻⁶ SI, forming the regional magnetic background field.

Remanent magnetization values (Figure 3d) range from 0 to 6000 × 10⁻³ A/m, spanning three orders of magnitude. Their intensity and stability depend on the type of ferromagnetic minerals and their formation environment [28]. Secondary magnetite and pyrrhotite formed during late-stage tectonic and hydrothermal processes are the primary contributors to the high remanent magnetization observed in calcite-biotite rocks, where values exceed 1000 × 10⁻³ A/m. In contrast, other lithologies generally show values below 500 × 10⁻³ A/m. According to the resistivity date (Figure 3e), rocks can be classified into four categories: low, medium-low, medium-high, and high resistivity. Unmineralized calcite-biotite rock, the host rock of niobium-magnetite mineralization, shows medium-low resistivity (mean 928.5 Ω·m; median 628.4 Ω·m). Calcite-bearing pyroxenite, amphibolite, and aegirine syenite show slightly higher values (typically 1000–1500 Ω·m). Diabase and diorite porphyrite exhibit high resistivity (2000–5000 Ω·m) but occur in limited volumes. Granitic gneiss shows low to medium-low resistivity, with a median of 566.0 Ω·m, the lowest in the study area.

Based on induced polarization (IP) intensity (Figure 3f), rocks can be grouped into low- and high-polarizability types. High polarizability is mainly associated with calcite-biotite rock, amphibolite, and diabase, reflecting the presence of sulfides such as pyrite. Other lithologies show low polarizability, generally below 5%. The average concentrations of K, U, and Th in the Dagele area are significantly higher than other regional backgrounds, indicating enrichment of radioactive elements in niobium-phosphorus ores and the influence of Devonian carbonatite intrusions and wall-rock alteration (second stage) [29].

The distribution of radioactive parameters (Figure 3g–j) indicates that aegirine syenite, intermediate-mafic intrusive rocks, and unmineralized calcite-bearing pyroxenite show no significant spectral anomalies, reflecting the absence of radioactive minerals; their K content mainly reflects the primary mineralogy. In contrast, pyrochlore-bearing calcite-biotite rock and amphibolite are affected by hydrothermal processes, resulting in enrichment in radioactive minerals and the corresponding spectral anomalies. Calcite-biotite rock is notably characterized by high uranium and low thorium and potassium contents. Granitic gneiss and some altered rocks display weak spectral anomalies, likely related to localized hydrothermal introduction of radioactive minerals.

3.2. Statistical Analysis of Physical Parameters for the Main Lithologies Using Histograms

The lithologies intersected in drill hole ZK3202 are relatively simple. Calcite-biotite rock, calcite-bearing pyroxenite, and amphibolite account for more than 85% of the total thickness, whereas all other lithologies are thinner, at less than 40 m, and are non-representative. Therefore, histogram analysis of physical property responses was performed only for the main lithologies. Based on core logging, lithologic intervals with complete stratigraphy, thicknesses greater than 200 m (chosen to ensure representative and continuous sampling), and clear mineralization anomalies were selected. After removing extreme values, five parameters sensitive to lithology and metallic mineralization were chosen: density, magnetic susceptibility, resistivity, polarizability, and total natural gamma [30]. Statistical histograms were then used to characterize the physical property distributions of the complex (Figure 4), providing data support for lithologic identification, stratigraphic subdivision, and mineral exploration.

Physical property statistics show that density, magnetic susceptibility, resistivity, polarizability, and total natural gamma for calcite-biotite rock (Figure 4a), calcite-bearing pyroxenite (Figure 4b), and amphibolite (Figure 4c) all display varying degrees of dispersion. Density, magnetic susceptibility, and polarizability exhibit high-value anomalies, whereas resistivity shows low-value anomalies, and total natural gamma presents a relatively high background. These patterns indicate significant mineralization and alteration anomalies that cannot be fully identified through core observation alone [31].

Calcite-biotite rock shows the highest density and magnetic susceptibility among the three lithologies, with strong dispersion, wide ranges, and multimodal, strongly asymmetric distributions. Density peaks at 3.0–3.2 g/cm³, and magnetic susceptibility locally peaks at 20,000–30,000 × 10⁻⁶ SI, which are local anomalous maxima and distinct from the median value of 3255 × 10⁻⁶ SI shown in Table 1, clearly differing from the unimodal distributions of calcite-bearing pyroxenite and amphibolite. Resistivity, polarizability, and natural gamma are relatively concentrated and unimodal. A small number of low-resistivity anomalies occur on the left side of the resistivity peak, while a few extremely high-polarizability values appear on the right side of the polarizability peak, and a broad high anomaly occurs on the right side of the natural gamma peak. All three lithologies show pervasive niobium and phosphorus mineralization, with calcite-biotite rock being the most enriched and commonly associated with disseminated and stockwork titanomagnetite and pyrrhotite mineralization. It is therefore characterized by high density, strong magnetism, low resistivity, high polarizability, and elevated natural gamma (Figure 4a).

The physical parameters of calcite-bearing pyroxenite are relatively concentrated, with nearly symmetric unimodal histograms. A few high-value anomalies occur on the right side of the density and magnetic susceptibility peaks, and some low-value anomalies on the left side of the resistivity peak, reflecting widespread mineralization and alteration association with pyrrhotite and limonite. Its characteristic physical property assemblage includes moderate density, moderate magnetic susceptibility, medium-high resistivity, low polarizability, and low total natural gamma (Figure 4b).

For amphibolite, density, magnetic susceptibility, resistivity, and natural gamma are relatively concentrated, although a small number of scattered natural gamma values and several high-value anomalies occur on the right side of the histogram. Polarizability is distinctly asymmetric and highly variable, likely related to pyrite and pyrrhotite mineralization. Overall, amphibolite is characterized by medium-high density, weak magnetic susceptibility, medium-high resistivity, relatively high polarizability, and moderate total natural gamma (Figure 4c).

Overall, the physical properties of rocks in the Dagele area show strong heterogeneity. Their distribution patterns are closely related to lithology, mineralization intensity, and multi-stage geological processes, as reflected by wide ranges of density and magnetic susceptibility, diverse electrical characteristics, and relatively elevated radioactive anomalies.

3.3. Correlation Analysis of Physical Parameters

To quantitatively characterize the relationships among rock physical parameters, Pearson correlation coefficient analysis was applied to eight parameters, including density, magnetic susceptibility, and resistivity (Figure 5) [32]. A positive correlation indicates that two variables increase together, whereas a negative correlation reflects an inverse relationship. The Pearson correlation coefficient was used to quantify the strength and direction of linear relationships between parameter pairs. The results reveal strong correlations among the parameters. Total radioactivity shows a strong positive correlation with uranium radioactivity. Magnetic susceptibility, polarizability, and density in the main lithologies, particularly calcite-biotite rock, show moderate positive correlation. This relationship is attributed to the paragenesis of magnetite and niobium-bearing minerals, supporting an ore-forming model involving rare element coprecipitation associated with Early Paleozoic hydrothermal activity [33]. The widespread occurrence of pyrite in the study area contributes to the relatively high polarizability values. Resistivity and polarizability also show a positive correlation in the study area. This relationship differs from the typical inverse correlation observed in many sulfide assemblages. Here, the coexistence of sulfide mineralization and intense hydrothermal alteration can increase both resistivity and polarizability simultaneously. However, the statistical analyses do not consistently support a strong coupling between high resistivity and high polarizability. In addition, density shows a positive correlation with thorium radioactivity, suggesting synchronous enrichment of pyrochlore, rare element minerals, and radioactive elements. These internal correlations among physical parameters provide further insights into the multi-stage metallogenic processes of the Dagele deposit.

3.4. Cross-Plot Analysis of Physical Parameters for the Main Lithologies

Based on the statistical analysis of physical properties, mean values were calculated to construct cross-plots of the main lithologies intersected by the drill hole (Figure 6). These cross-plots illustrate the distribution characteristics of the three lithologies [34]. Type 1 (red dots): high density, strong magnetic susceptibility, high polarizability, medium-low resistivity, and moderately high total radioactivity, corresponding to calcite-biotite rock. Type 2 (blue dots): medium-high density, moderate magnetic susceptibility, medium-high resistivity, low polarizability, and low total radioactivity, corresponding to calcite-bearing pyroxenite. Type 3 (green dots): moderately high density, low magnetic susceptibility, medium-high resistivity, moderately high polarizability, and moderate total radioactivity, corresponding to amphibolite. In Figure 6b, the red and green clusters partly overlap, indicating that polarizability alone has limited ability to distinguish between calcite-biotite rock and amphibolite, although it is effective for identifying calcite-bearing pyroxenite. However, the combined use of five parameters—density, magnetic susceptibility, resistivity, polarizability, and total radioactivity—allows reliable discrimination among the three lithologies.

3.5. Physical Property Response Characteristics and Identification of Mineralized and Altered Zones

Based on lithophysical statistics and cross-plot interpretation, key parameters, including density, magnetic susceptibility, remanent magnetization, resistivity, polarizability, and total radioactivity (U, Th, K), were integrated with core logging data to construct a lithologic interpretation profile of physical parameters for drill hole ZK3202 (Figure 7). The profile also indicates the locations and numbers of physical property samples. The interpreted profile shows the lithologic distribution along the borehole: 0–190 m is dominated by amphibolite, interbedded with diorite porphyrite and diabase, with well-developed alteration zones; 190–470 m is dominated by calcite-bearing pyroxenite, associated with aegirine syenite, diabase, and multiple layers of calcite-biotite rock; 470–610 m consists mainly of amphibolite with veined diorite porphyrite and aegirine syenite; 610–980 m represents a transitional zone between calcite-biotite rock and calcite-bearing pyroxenite, locally cut by veins of aegirine syenite and diabase; from 980 m to the end of the borehole, amphibolite dominates, with progressively coarser grain size toward the bottom. This profile clarifies the stratigraphic framework, lithologic boundaries, and spatial distribution of mineralized and altered zones, providing key geological constraints for identifying and delineating mineralized intervals [35].

Wall-rock alteration in the Dagele niobium deposit is mainly characterized by carbonatization and phlogopitization. Niobium mineralization occurs in disseminated and stockwork forms within altered rocks, and the ores contain abundant sulfides, ferromagnetic minerals, and radioactive minerals, such as those specified in [36]. Previous studies indicate that the core zone of carbonatization–phlogopitization coincides with the niobium enrichment zone. Metallic minerals increase density, hydrothermal magnetite enhances magnetic susceptibility, mineral compaction influences resistivity, sulfide alteration produces zoned polarizability, and pyrochlore and related minerals increase radioactivity. The co-enrichment of Fe-Ti-bearing magnetic niobium minerals strengthens magnetic anomalies and produces superimposed medium-low resistivity signatures [37]. Magnetitization, pyritization, and columbitization are the main mineralization types and are responsible for significant variations in physical parameters. Magnetitization is associated with high magnetic susceptibility and high remanent magnetization; pyritization corresponds to high polarizability; and columbitization corresponds to medium-low resistivity and high density, generally occurring together with the former two types of mineralization.

Based on mineralization and alteration features and their physical property responses, mineralized and altered zones were identified within the calcite-biotite rock, calcite-bearing pyroxenite, and amphibolite intervals of drill hole ZK3202 at depths of 710–870 m, 180–370 m, and 470–580 m, respectively (Figure 8;

Table 2. Statistical table of typical mineralized alteration zones and their physical properties.

Lithological	Physical Property Position/m	Mineralization Type	Density /g/cm3	Magnetic Susceptibility /10−6 SI	Resistivity /Ω·m	Polarizability /%	U Content /10−6	Th Content /10−6	K Content /%	Total Radioactivity /API
calcite-biotite rock	732.8	magnetitization /pyritization /columbitization	3.22	17,733	2388.7	10.42	4.98	15.2	1.35	18.8
	734.1	magnetitization /pyritization /columbitization	3.03	37,767	945.9	22.36	4.23	14.8	1.40	18.6
	742.6	magnetitization /pyritization /columbitization	3.45	27,467	1670.9	6.68	4.95	13.4	1.30	18.5
	783.5	magnetitization /pyritization /columbitization	3.77	31,400	2729.0	17.93	4.57	13.7	1.03	17.5
	801.5	magnetitization /pyritization /columbitization	3.92	72,267	4554.6	26.19	9.37	13.0	1.27	22.7
calcite-bearing pyroxenite	207.5	magnetitization /columbitization	3.20	2541	2488.6	1.26	4.28	13.0	1.40	17.8
	219	pyritization	3.19	317	6069.4	10.57	4.58	13.3	1.30	17.9
	289.2	pyritization	3.07	470	5890.6	7.21	5.88	13.7	1.30	19.1
	356.7	magnetitization /columbitization	3.11	7080	1763.4	1.43	4.15	12.8	1.50	17.7
	363.8	magnetitization /columbitization	3.25	2510	1855.6	1.44	4.00	13.0	1.45	18.0
amphibolite	484.3		3.62	782	2415.5	1.85	4.98	11.8	1.25	17.7
	492.1		2.42	86	947.0	0.49	5.75	14.0	1.20	17.6
	515.8	magnetitization	3.07	3233	1076.8	3.52	2.78	15.0	1.28	17.1
	562.8		2.98	509	1132.4	1.78	4.68	13.0	1.25	17.7
	569.3		2.87	146	1327.6	2.02	5.18	12.9	1.25	18.1

).

The high polarizability value (up to 26.19%) observed in calcite-biotite rock is related to disseminated sulfides and hydrothermal alteration and is supported by borehole measurements. Strongly mineralized intervals show high magnetic susceptibility, high polarizability, and medium-low resistivity (Figure 8a), locally accompanied by high density and elevated radioactivity. These features reflect high contents of magnetite, pyrite, and columbite, with local pyrochlore mineralization. Calcite-bearing pyroxenite exhibits medium-high resistivity (Figure 8b), with variable density and magnetic susceptibility. Magnetite–columbite intervals correspond to moderate magnetic susceptibility, whereas high pyrite contents are associated with elevated polarizability. Amphibolite intervals are characterized by low magnetic susceptibility, low polarizability, low radioactivity, and medium-high resistivity (Figure 8c). Overall, the physical parameters show strong correlations with mineralization and alteration processes [38,39].

4. Discussion

Niobium has extremely low abundance in the continental crust and rarely produces a distinct geophysical anomaly by itself. It mainly occurs as pentavalent oxides (Nb, Ta)₂O₅ in minerals such as columbite and pyrochlore, which exhibit characteristic physical properties [40]. Based on continuous multi-parameter physical measurements along drill hole ZK3202, combined with core logging, sample analyses (

Table 3. The location and core test results of core samples of hole ZK3202.

Geochemical Sample No.	Sampling Location/m		Thickness /m	Analysis Result	Ore Body No.
	Top Depth	Bottom Depth		(Nb, Ta)2O5/%
H2~H4	189.11	193.1	3.99	0.032
H7~H10	196.06	201.26	5.2	0.023
H11~H17	201.26	211.76	10.5	0.065	M1-1
H18~H50	211.76	260.92	49.16	0.028
H51~H62	260.92	278.81	17.89	0.107	M1-2
H63~H101	278.81	337.31	58.5	0.033
H102~H124	337.31	371.66	34.35	0.062	M1-3
H125~H128	371.66	377.31	5.65	0.044
H129~H142	377.31	397	19.69	0.088	M1-4
H143	397	398.5	1.5	0.014
H147~H153	403	412.8	9.8	0.077	M1-5
H154~H160	412.8	423.3	10.5	0.039
H161~H172	423.3	442.3	19	0.061	M1-6
H173~H176	442.3	448.7	6.4	0.021
H177~H188	448.7	466.61	17.91	0.142	M1-7
H189~H193	466.61	474.93	8.32	0.025
H196~H200	612.40	620.30	7.9	0.025
H201~H214	620.30	641.30	21	0.165	M2-1
H222~H231	652.45	667.45	15	0.034
H232~H236	667.45	674.95	7.5	0.070	M2-2
H237~H248	674.95	692.95	18	0.038
H249~H253	692.95	700.32	7.37	0.106	M2-3
H254~H272	700.32	728.82	28.5	0.042
H273~H295	728.82	763.30	34.48	0.167	M2-4
H296~H305	763.30	778.30	15	0.035
H306~H365	778.30	867.50	89.2	0.125	M2-5
H366~H369	867.50	873.50	6	0.027
H374~H388	878.85	901.60	22.75	0.037
H389~H397	901.60	914.80	13.2	0.063	M5-1
H400~H411	918.50	937.15	18.65	0.067	M5-2
H412~H440	937.15	979.80	42.65	0.026

Note: Values of (Nb, Ta)₂O₅ < 0.01% are not included in this table; those falling within the range of 0.01% ≤ (Nb, Ta)₂O₅ < 0.05% are left unnumbered.

), and comprehensive geological investigations, this study establishes prospecting criteria for identifying favorable niobium mineralization intervals using multi-parameter geophysical methods [41,42] and summarizes the multi-parameter coupling mechanism of ore-bearing lithofacies [43].

4.1. High-Density, High-Magnetic Anomaly Zones as Indicators of Favorable Niobium Mineralization

This section integrates lithophysical characteristics and multi-parameter geophysical anomalies to establish prospecting criteria for niobium mineralization. Similar lithophysical approaches have been applied in the Zhezkazgan ore district (Central Kazakhstan), particularly for deep mineralization targeting, and are methodologically consistent with this study.

Geological evidence indicates that orebodies in the Dagele deposit are mainly located in the central part of the complex, with calcite-biotite rock as the dominant ore-bearing lithology, accompanied by minor pyroxenite, typical of alkaline rock–carbonatite-type niobium deposits. Core physical property data (Table 2) show that calcite-biotite rock in drill hole ZK3202 is characterized by high-density and high-magnetic susceptibility (and remanent magnetization), medium-low resistivity, and high polarizability, whereas other lithologies generally display lower or contrasting values.

Nine anomaly zones are identified along the borehole (Figure 9), defined by high density, strong magnetism, medium-low resistivity, and high polarizability. Zones ①, ②, ③, and ⑦ represent high-density transitional zones with moderate magnetic anomalies and low to medium-high polarizability, corresponding to calcite-bearing pyroxenite with relatively low contents of magnetite, pyrite, and columbite. In contrast, zones ④, ⑤, ⑥, ⑧, and ⑨ exhibit high density, strong magnetic anomalies, medium-low resistivity, and high polarizability, corresponding to calcite-biotite rock enriched in magnetite, pyrite, and columbite. Among these, zones ②, ③, ⑥, ⑦, and ⑧ are additionally characterized by high uranium and total radioactivity, along with low thorium and potassium contents [44].

Combined with core analyses, Nb grades range from 0.014 to 0.142% and show a positive correlation with geophysical parameters (e.g., polarizability, resistivity, and magnetic susceptibility), supporting orebody delineation. Several orebodies (M1-1 to M5-2) were identified within zones ①–⑨. Transitional anomalies in density, magnetic susceptibility (including remanent magnetization), polarizability, resistivity, and natural gamma effectively delineate three main orebodies: M1, M2, and M5. Thus, in drill-hole exploration of the Dagele niobium deposit, lithological identification and recognition of transition zones using density–magnetic susceptibility–polarizability profiles can indirectly indicate favorable ore-hosting positions. Accordingly, anomalies in density, magnetic susceptibility, resistivity, and polarizability, locally supported by uranium and total radioactivity, constitute effective geophysical criteria for prospecting in this area.

4.2. Multi-Parameter Coupling Mechanism of Ore-Controlling Lithofacies and Its Exploration Significance

As the principal ore-hosting lithofacies, the physical properties of calcite-biotite rock are jointly controlled by mineral composition, texture and structure, as well as late-stage hydrothermal alteration [45], forming a coupling relationship in which “physical properties dominated are ferromagnetic minerals, while element distribution is controlled by fluid activity” [46]. Enrichment in heavy minerals such as columbite and pyrochlore leads to high density. High magnetic susceptibility and high remanent magnetization are mainly controlled by ferromagnetic minerals and are positively correlated with niobium-related hydrothermal activity, showing clear contrasts with surrounding wall rocks. The assemblage of medium-low resistivity and high polarizability is governed by the combined effects of conductive and insulating minerals as well as interfacial polarization and is positively correlated with the intensity of hydrothermal alteration, making it a typical indicator of mineralized and altered zones. The elemental assemblage characterized by medium-high U and total radioactivity, together with low Th and K, reflects the combined influence of protolith composition, metamorphic differentiation, and ore-forming fluid activity. Uranium enrichment is broadly synchronous with niobium mineralization and can therefore serve as an indirect indicator of niobium mineralization.

These physical property contrasts provide a reliable basis for geophysical exploration. High density serves as a direct indicator for gravity surveys; medium-low resistivity and high polarizability help delineate targets in resistivity and IP surveys, strong magnetic anomalies help distinguish mineralized bodies from magnetic igneous rocks, and radioactive anomalies indicate the degree of niobium mineralization. Integrated multi-parameter analysis thus significantly reduces the ambiguity of anomaly interpretation [47].

4.3. Physical Prospecting Criteria, Integrated Model and Regional Application Value

The physical property assemblage of calcite-biotite rock provides multi-parameter criteria for deep prospecting and target delineation of the Dagele niobium deposit [48]. Integrated anomaly zones characterized by high density (>3.0 g/cm³), high magnetic susceptibility (>1000 × 10⁻⁶ SI), high remanent magnetization (>1000 × 10⁻³ A/m), medium-low resistivity (10²~10³ Ω·m), and high polarizability (>5%) are identified as direct geophysical indicators of niobium mineralization. The elemental assemblage of medium-high uranium (>5 × 10⁻⁶), medium-high total radioactivity (>18 × 10⁻⁶), low thorium (<13 × 10⁻⁶), and low potassium (K₂O < 1.25%) can be used to identify mineralized and altered rocks from non-mineralized wall rocks. Based on these features, a three-in-one prospecting model of “high density–strong magnetism–medium-low resistivity and high polarizability–uranium radioactivity anomaly” is established. This model is consistent with the physical property characteristics of ore-forming parent rocks in similar niobium deposits worldwide. It can therefore serve as an effective indirect prospecting criterion for carbonatite-alkaline rock-type niobium deposits in the Eastern Kunlun region and provides a geophysical basis for preliminary regional target delineation.

This study supplements the physical property database of niobium deposits in the Eastern Kunlun orogenic belt and addresses the previous lack of systematic physical property studies on the complex tectonic settings of western China. The results provide a useful reference for niobium exploration in similar metallogenic belts, such as those of the northern Qinghai-Tibet Plateau, and contribute to the development of geophysical prospecting models for alkaline rock-type niobium deposits in western China.

4.4. Limitations and Future Work

The samples analyzed in this study were mainly collected from a single drill hole, and systematic investigations of the physical properties of surface samples and mineralized bodies from multiple deep drill holes have not yet been conducted. In addition, the limited number of samples restricts the analysis of physical property variations associated with different stages and intensities of mineralization.

Future work will include additional physical property measurements on surface samples and deep samples from multiple drill holes, as well as detailed analyses of the relationships between mineralization intensity and physical parameters. Combined with comprehensive ground gravity, magnetic, electrical, and radioactive geophysical surveys as well as laboratory measurements will be integrated with field geophysical anomalies to develop a robust geophysical prospecting model for the Dagele niobium deposit, providing more accurate technical guidance for exploration deployment in the study area.

5. Conclusions

Based on geophysical property data from the Dagele niobium mining deposit in the Eastern Kunlun region, this study analyzes the physical property characteristics of wall rocks, mineralized zones, and orebodies. Combined with core logging, sample testing, and comprehensive geological analysis, multi-parameter prospecting criteria for favorable niobium mineralization intervals are established, the coupling mechanism of physical property in ore-hosting lithofacies is summarized, and its exploration significance is discussed. The main conclusions are as follows:

• Using box plots, lithological histograms, and correlation coefficient heatmaps, five parameters (density, magnetic susceptibility, resistivity, polarizability, and total natural gamma) are shown to effectively distinguish the three main lithologies. Geophysical properties therefore provide a reliable basis for reconstructing drill-core profiles in niobium exploration.
• Mineralized intervals are identified and classified using cross-plot techniques. The physical property distributions of different mineralized and altered zones are analyzed, and multi-parameter prospecting criteria for favorable niobium mineralization intervals are established. The multi-parameter anomaly zone defined by a density > 3.0 g/cm³, magnetic susceptibility > 1000 × 10⁻⁶ SI, remanent magnetization > 1000 × 10⁻³ A/m, resistivity of 10²~10³ Ω·m, polarizability > 5%, uranium > 5 × 10⁻⁶, total radioactivity > 18 × 10⁻⁶, thorium content < 13 × 10⁻⁶, and K₂O < 1.25%, is identified as the primary target for niobium mineralization.
• The ore-hosting lithofacies, calcite-biotite rock, exhibits a characteristic physical signature of high density, strong magnetism, medium-low resistivity with high polarizability, and medium-high uranium radioactivity, clearly distinguishing it from the surrounding wall rocks. This provides a direct physical basis for integrated gravity-magnetic-electrical-radioactive geophysical exploration and accurate delineation of mineralization targets.
• The key geophysical physical parameters obtained in this study fill a gap in the physical database of carbonatite-alkaline rock-type niobium deposits in the Eastern Kunlun region. Similar lithophysical discrimination and multi-parameter prospecting frameworks have been successfully applied in other metallogenic provinces worldwide, indicating that the criteria established here are not only deposit-specific but also consistent with broader trends in exploration geophysics. They provide a reference for exploration and metallogenic prediction of similar niobium deposits in the Eastern Kunlun orogenic belt and western China, contributing to the improved efficiency of niobium exploration in the region.