چكيده لاتين
TheWest Band Narges-e iron ore deposit is located west of the Band Narges iron mine, approximately 70 kilometers from the city of Badroud, in the northeastern part of the 1:100,000-scale Kuh-e Latif geological map. The oldest geological unit in the area is Cretaceous limestone, which appears in the central part of the region in a light cream color. Extensive Eocene volcanic rocks, composed mainly of andesite, have developed across the region and, together with the limestone units, form the host rocks for mineralization. These volcanic units rest discontinuously atop the Cretaceous limestone. A light-colored granodioritic intrusive body, trending northwest–southeast and dated to the Eocene–Oligocene, is exposed in the southern and central parts of the area. This intrusive body, along with its late-stage offshoot dikes, has intruded into both the Eocene volcanic units and the Cretaceous limestone. This granodioritic body is overlain discontinuously by the Lower Red Formation (Oligo-Miocene in age), which is exposed in the northern part of the study area. Above this, in the northern zone, lies the Qom Formation (also Oligo-Miocene), which appears as a white-colored, discontinuous unit. In the northern portion of the study area, Neogene gypsum and marl units rest unconformably on older strata. Finally, Quaternary alluvial deposits, such as windblown sands and gravels, cover older formations and are most commonly observed in the southern and northern regions. In the northern part of the study area, a fault zone with an east–west to northwest–southeast orientation, and a compressive–dextral strike-slip movement, has displaced Eocene andesitic units over the conglomeratic deposits of the Lower Red Formation, as well as over the tuffs and limestones of of the Qom Formation. A similar fault zone with a comparable trend and mechanism is observed in the southern part of the area, where faulting has caused Eocene volcanic rocks to thrust over younger Miocene to Quaternary sediments. The intrusive body of the area displays characteristics of magmas associated with subduction zones. The origin of the magma is mantle-derived, with some evidence of crustal contamination. Geochemical data indicate enrichment in LILE and LREE elements and depletion in HFSE and HREE elements. There are three main mineralized veins in the area, with high-grade mineralization occurring primarily in limestone units, while volcanic units exhibit vein-type mineralization. Overall, the deposit contains approximately 1.4 million tons of iron ore with an average grade of 50%. Propylitic alteration appears green in the northern part of the area, argillic alteration is light yellow in the central and southern regions, and phyllic alteration, in a creamy yellow hue, outcrops in the central part. Magnetite, hematite, pyrite, and chalcopyrite are the dominant ore minerals, while garnet, quartz, and calcite are the most abundant gangue minerals. The formation of this deposit occurred through three key stages: prograde, retrograde, and supergene. Garnet formed during the prograde stage, while magnetite, pyrite, and chalcopyrite developed during the retrograde stage. In the supergene stage, goethite and covellite replaced pyrite and chalcopyrite, respectively. Fluid inclusion studies on five quartz and garnet samples indicate salinities ranging from 3 to 40 wt% NaCl and formation temperatures between 120°C and 392°C. The maximum depth and pressure of ore formation are estimated at 1.2 km and 30 MPa, respectively. Boiling and mixing of fluids played a significant role in ore formation. The primary fluid was magmatic, which mixed with meteoric waters in later stages. The δ¹⁸O values for five quartz samples range from –2.3‰ to +6.3‰, suggesting a lighter isotopic signature than typical magmatic sources. This is attributed to the enrichment of lighter isotopes in magnetite compared to silicate minerals.
