## 3 Results and Discussion  
During data processing, the entire 5200 m profile was subjected to inversion analysis. The central 2000 m segment of the inversion results was then extracted, yielding resistivity and chargeability cross-sections extending to depths of 1200 m below the surface. Figures 4 and 5 present the resistivity/chargeability inversion results for line L1. The inversion reveals transitional zones between stations 520-620 and 920-1000, likely caused by fracture zones. The resistivity inversion shows minimal near-surface variations, with a 50-150 m thick low-resistivity layer interpreted as clay-rich weathering products. A dike-like high-resistivity anomaly occurs between stations 700 and 850, possibly representing intrusive granitic porphyry or quartz porphyry. Two high-chargeability anomalous zones are identified at stations 80-440 and 950-1100, with shifting anomaly centers flanking the high-resistivity dike and corresponding to low-resistivity zones in the resistivity section. Based on spectral IP characteristics of metallic deposits, the IP anomalies at stations 400 and 1000 most likely originate from massive metallic mineralization, exhibiting typical metallic deposit signatures and potentially representing skarn-type or quartz-vein polymetallic deposits. Figure 4: Two-dimensional inversion of the resistivity of the L1 line. The burial depth of the igneous rock top interface gradually becomes shallower from the small mileage to the large mileage direction, with the shallowest granite top interface occurring at about 200 m depth in the section from 1400 m to 1600 m of L1. Based on the resistivity and chargeability anomaly characteristics, the low-resistivity anomaly zones that developed within high-resistivity areas or near high-resistivity anomalies are interpreted as ore veins. So, three ore veins are identified in the L1 geological profile (Figure 6): The skarn-type (Vein A) is located at the contact between volcanic rocks and sedimentary rocks in the section from 200 m to 400 m of L1, showing low-resistivity and high-polarization features with its top interface around 0 m elevation. The greisen-type (Veins A and B) occurs at the contact zone between igneous rocks and sedimentary rocks: Vein B in the section from 500 m to 700 m of L1, exhibiting low-resistivity and high-polarization characteristics with its top interface near 50 m elevation; and Vein C in the section from 850 m to 1100 m of L1, demonstrating low-resistivity and moderate- to low-polarization properties with its top interface at approximately 200 m elevation. The resistivity/chargeability inversion results for Line L2 are presented in Figures 7 and 8. Between stations 200 and 650, a high-resistivity layer exists beneath the surface, likely caused by shallow quartz sandstone, siltstone, or marble. Below this high-resistivity layer lies a low-resistivity zone, interpreted as Devonian mudstone or shale. A steeply dipping high-resistivity body occurs between stations 740 and 900, possibly representing an intrusive granite dike. The first IP anomaly zone (between stations 700 and 760) exhibits high chargeability and corresponds to a low-resistivity anomaly in the resistivity section, distributed near the intrusive dike and attributed to massive metallic mineralization. The second induced polarization anomaly, located between stations 300 and 500, exhibits a high-resistivity and low-chargeability signature, which is interpreted as limestone in contact with intrusive granite. Figure 5: The results of the two-dimensional inversion of the L1 linear width frequency. Figure 6: Interpretative geological profile of L1. 1: Weather layer/quaternary sediments; 2:’sandstone/sandy mudstone; 3: Devonian limestone; 4: medium-fine-grained porphyritic biotite granite; 5: skarn-type W-Sn orebody and its identification letter; 6: greisen-type W-Sn orebody and its identification letter; 7: greisen-type W-Sn orebody and its identification letter. Figure 7: Two-dimensional inversion of the resistivity of the L2 line.