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13GENERAL CHARACTERISTICS PISTALI DEPOSITS
Tolib Sirozhevich Amanov
Uzbek Institute Of Geotechnical And Non-Ferrous Metallurgy Research And Project Search "O'zgeorangmetliti"
Engineer of The Mining Department of the State Unitary Enterprise
Azamat Abdurashidovich Umirzoqov
Tashkent State Technical University named after Islam Karimov
G'ayrat Alimansurovich Xatamov
Student Tashkent State Technical University named after Islam Karimov
Yulduzoy Alfazar qizi Mirzayeva
Student Tashkent State Technical University named after Islam Karimov
ABSTRACT
According to the administrative division, the Pistali field belongs to the Nuratinsky district of Navoi region, 30 km north-east of Nurata, and 90 km from Navoi. The paved Navoi - Nurata - Jizzakh road runs in the northern edge of the field area. The Pistali deposit is located on the northern slopes of the western end of the Northern Nuratau Mountains, which pass to the north into the plain with Lake Aidarkul.
Keywords: Pistali, mining, deposits, open pit mining, geological structure.
INTRODUCTION
The terrain is poorly dissected, with absolute marks from + 390 to 410 m, less often up to 430 m. The climate of the area is sharply continental with long hot summers and short snow-free winters. Temperature fluctuations in summer from plus 15 to plus 45 0C, in winter-from plus 12 to minus 30 0C. Frequent strong winds (up to 15 m/s) and dust storms are typical. The average annual precipitation is 320 mm, the maximum -500 mm.
METHODOLOGY
There are no permanent watercourses. For drinking water supply, water from artesian wells drilled in the village is mainly used [1-4]. Kyzylcha, located 17 km east of the Pistali field. The power supply is provided from a 35 kW transmission line running along the northern border of the field. Dangerous manifestations of mudslides, landslides are not noted. The seismicity of the area is up to 5-6 points on the Richter scale [5-7].
Geological structure of the deposit
The Pistali deposit is located in the western part of the Northern Nuratau ridge, which in geotectonic terms belongs to the Kyzylkum middle massif, to its eastern flank. The boundary of the middle massif and the folded system of the eastern extension of the ridge is a powerful diagonal zone of the Majerum fault, identified on geological maps at a scale of 1:50000 west of the Koshrabad intrusive and the Zarmitan deposit. The central Kyzylkum uplands and the western part of the ridge are united by powerful Precambrian terrigenous complexes of the Taskazgan and Besapan formations, powerful granitization, polyfacial regional metamorphism, and gold mineralization of the type of shallow mineralized zones [8].
Structurally, the Pistali deposit is confined to the western periclinal closure of the Yambash-Ustuk brachianticline with a length of 70 km and a width of up to 15 km. The azimuth of the anticline axis is 280-290°, the angle of immersion of the hinge is 10°-30°. The northern part of it is dumped and buried under the proluvial quaternary sediments of the Golodnostep complex and shallow marine sediments of the Paleogene, according to the system of Alpine breaks. The arched part of the brachianticline is deeply eroded, its core is composed of rocks of the Taskazgan formation, the southern wing-rocks of the Besapan formation. The rocks are metamorphosed at the level of the green-shale facies and partially of the epidote-amphibolite facies in the form of separate horizons of green quartz-albite-chlorite (metatufs), albite-clinocoisite-chlorite-amphibole (metabasalts) and crystalline schists.
To the east of the site, the large Temirkabuk granitoid massif is located in the core of the brachianticline, followed by the Ustuk and Sentyabsky massifs [9]. All of them bear signs of autochthonous formation due to the melting of the original sedimentary-metamorphic rocks. In the western and northern frames of the site, according to the data of the gravimagnetic survey, the hidden Kulkuduk massif of acid composition was identified, which is an ore-generating granitization center that determined the position of the deposit [10].
It is assumed that the Yambash-Ustukskayabrahi anticline with a gentle occurrence of rocks in the area of the sinking hinge and a steep occurrence on the wings, is a consequence of the formation of an area of autochthonous granitoids of the laccolith type lying in its core.
Against the general background of the simple structure of the brachianticline in the deposits of the Taskazgan formation, a complex system of fragments of isoclinal and underlying folds of different orders, up to flatness, is widely developed, which is strongly obscured by zones of intense schistation (tectonization) of rocks. This form of early tectogenesis corresponds to the type of zones of horizontal scaly thrusts or plastic dislocations that rebuilt the original folded appearance of the Taskazgan formation.
Metasomatic changes in rocks and ore mineralization are associated with such zones of increased permeability [11].
The discontinuous tectonics in the area is mainly represented by longitudinal discontinuous faults extending 290-300°, largely healed by lamprophyre dikes and quartz veins. Some of the fractures are accompanied by metasomatic changes in rocks with interspersed sulfide mineralization. In the most powerful and extended steep-falling zones of longitudinal breaks within the Besapan formation, the ore occurrences of the Kansai gold-bearing zone are located. Diagonal shear discontinuities are also noted [12-15].
In general, the deposits of the Taskazgan and Besapan formations in the western part of the Northern Nuratau ridge are associated with a large number of gold ore occurrences and placers, as well as numerous geochemical halos of gold scattering.
In genetic and morphostructural terms, there are two types of gold mineralization: the type of shallow ore deposits identified at the Pistali deposit, and the type of intermittent veins and veined quart formation in the zones of steeply falling longitudinal discontinuities at the Kansai, Kulkuduk, etc. ore occurrences. To date, industrial concentrations of gold in the latter have not been established [16-18].
The geological structure of the Pistali deposit and its flanks for 8 km from east to west, includes sedimentary-metamorphosed rocks of the Upper Proterozoic Taskazgan formation (RR2ts), represented by mica-quartz and muscovite-sericite shales, metaaleurolites, metapesanites and quartzites, broken dikes of diorite porphyrites, granodiorite-porphyry and Pistali stock of quartz rocks.syenite-diorites of the Kattaichi middle carboniferous complex [19].
To a large extent, the rocks are overlain by deluvial-proluvial deposits of the Golodnostep Quaternary complex. The wells in the northern part of the area contain Paleogene deposits.
The Taskazgan formation is represented by two sub-formations: the lower and the upper. The rocks of the lower sub-formation comprise most of the area of the Pistali site and its flanks. It consists of five bundles (from the bottom-up along the section and from east to west).
The Taskazgan formation is represented by two sub-formations: the lower and the upper. The rocks of the lower sub-formation comprise most of the area of the Pistali site and its flanks. It consists of five bundles (from the bottom-up along the section and from east to west) [20-24].
Pack 2 is essentially carbon-shale in composition. Subordinate interlayers and bundles of metapeschanics and metaaleurolites. There are horizons and individual layers of metasilicate quartzites associated with dolomites and limestones with a thickness of
1-2 m to 5-20 m. The power of the pack is 200-400 m, the pack is ore-containing for ore deposits 1, 2, 3, 3-1, 3-2, 4.
Pack 3 is composed of metapestites, metaaleurolites, quartz-mica and mica-quartz schists with a thickness of up to 150 m.
The 4-carbon - siliceous (quartzite) - shale pack. Quartz-mica and mica-quartz carbonaceous and substantially carbonaceous shales predominate. Less developed are metaaleurolites and metapesanics. Numerous horizons of metasilicate quartzites are characteristic, sometimes in association with dolomites[25]. The power of the horizons from the first meters to 20-30m in inflations. Pack capacity up to 300 m.
Pack 5 is composed of metaaleurolites, metapesanites, quartz-mica and mica-quartz shales, sometimes carbonaceous to substantially carbonaceous with subordinate horizons of metacilicate quartzites, sometimes associated with dolomites and green chlorite-epidote shales. The thickness of the horizons is from the first meters to 20-50 m. The power of the pack is 600-800 m.
DISCUSSION
The Verkhnetaskazgan sub-formation forms the western part of the square. The defining component of the sub-formation is the numerous horizons of metasilicate quartzites, marbled limestones, and dolomites ranging in thickness from fractions of a meter to several tens of meters. The most powerful is developed at the base of the subformation and is represented by a bundle of interlayers of limestones with quartzites and dolomites. Blow-up capacity up to 150 m. Most of the sub-formation is composed of albite-porphyroblastic mica-quartz, crystalline muscovite-feldspar-quartz shales, gneisslike rocks, green quartz-albite-chlorite (metatufs) and albite-clinocoisite-chlorite-amphibole (metabasalts) shales, areas associated with ferruginous rocks (quartzites). Thickness of the thickness is 1500 m.
Paleogene deposits are developed in the northwestern buried part of the area. With an angular disagreement, they lean on the deposits of the Taskazgan formation. They are represented by the Upper Eocene, composed of quartz-muscovite sandstones, areas with gravel admixture, with interbeds of clay shale. The thickness of the sediments is from 1.5-2.0 m to 20 m, increasing in the north-east direction. They are completely blocked by deposits of the Holodnostep age. Installed on wells and pits in the northern part of the field area.
Quaternary deposits of the Tashkent complex are developed only in the northwestern part of the search area. With angular disagreement, the sediments of the Paleogene and the Taskazgan formation are overlaid. The thickness of the deposits is 10-20 m.
The quaternary deposits of the Golodnostep complex with angular unconformity overlap with the deposits of the Taskazgan formation. Their power ranges from 1-2m in the southern part of the site to 10-25 and 40 m in the northern part. According to the genesis, these are deluvial-proluvial deposits. By composition-loam with an admixture of crushed-gravel material. In the northern part, it is mainly sand and gravel deposits with an admixture of boulders and clay material [26].
Igneous rocks in the area of the deposit are represented by dikes of diorite and granodiorite compositions, which form a belt up to 1400 m wide directly on the area of the deposit and the Pistalinsky stock of quartz syenite-diorites. The strike of the dike belt is generally consistent with the strike of the host rocks. The dikes are composed of lamprophyritic diorite porphyrites of the spessartite and kersantite types (predominate) and granodiorite porphyries. Spessartites are earlier members of the series and are dissected by kersantites. Granite dikes are very rare. The power of dikes is from the first tens of cm to 20-30 m. The dike drop is mostly steep, more often with a drop to the west at an angle of up to 60-800. Less often, there are falls of rocks to the east and gentle (up to 20-500) occurrences. The rocks in the contacts are gneissized, the areas are marked by hardening zones [27].
The Pistalinsky stock is located in the southern part of the square and is confined to the central part of the dike belt. The shape of the array is lenticular in plan. The body measures up to 0.5 km in width and up to 1.5 km in length. Body stretch 350-3600. The main part of the massif is composed of quartz syenite-diorites. Earlier quartz monzonite-diorites are developed in the edges. The igneous rocks of the deposit area are attributed to the Kattaichi Middle Carboniferous complex.
It should be noted that the dikes break off at the northern end of the rod, without being traced inside it.
RESULTS
According to gravimagnetic data, the Kulkuduk hidden granitoid massif was identified to the west and north of the Pistali site (Norkulov et al., 1998). The shortest distance from the day surface to the roof of the intrusions is 500-700 m. Structurally, the field is confined to the nuclear part of the Yambash-Ustuk brachianticline. Immersion of the hinge of the anticline according to az. 290-300° with an angle of inclination from 100 to 300. The occurrence of rocks in the core of the fold has angles of incidence from 20 to 700, often with elements of tilting. The wings of the fold are complicated by numerous small folds with gentle hinges. The axial planes of the small folds are inclined in the direction opposite to the slope of the stratification-schist. Their development is probably associated with folding, which has a regional
development. The stretch of the axial planes of small folds is sustained over the entire area, is 330-3400, and is fixed by shading on the planes of shale.
The northern wing of the Yambash-Ustuk anticline is cut off by Alpine discontinuities. According to the drilling data, the presence of flat "recumbent" folds with a span from fractions of m to tens of meters was established. The folds are established by changing the orientation of the roof-sole of the layers in the rhythmically constructed metaterrigenous formations of the field area[28].
These folds are earlier in relation to the brachianticline. Discontinuous violations. The most recent longitudinal structures are more clearly recorded. Morphologically, these are steep-falling discharges, upturns. The zones of these ruptures are expressed by mylonitization, quartz formation, and sometimes are healed by quartz veins.
The largest longitudinal faults in the region include the zone of the North-Nuratinsky deep fault and its virgations, which run along the northern foot of the ridge and capture the surface of the young platform. The surfaces of the fault displacers are inclined to the south and southwest at angles of 60-800. The rupture zones are clearly marked by mylonitization, brecciation, and significant ozheleznenie. These structures are developed in the northern part of the deposit area and are largely overlain by the cover of quaternary sediments.
Within the limits of the deposit, discontinuities are recorded, the longitudinal axes of the brachianticline extending 275-2900. By nature, these are right shifts with an offset amplitude from the first meters to 100-150 m. The thickness of the break zones is from fractions of a meter to 10-15 m. Elements of the upsetting component are likely. The slope of the displacement plane is steep to the southwest (70-800). The fractures are represented by zones of crushing, ozheleznenie and raslantsevaniya, less okvartsevaniya.
Numerous shallow cracks and zones of dynamometamorphism are established along the pits and underground mine workings, which correspond to the orientation of the shale content of the host rocks, coincide with the zones of mineralization and define their boundaries. Sometimes they are accompanied by zones of encrustation [29]. A characteristic feature of the section of the lower sub-formation of the Taskazgan formation is the absence of pre-ore and intra-ore crushing textures. All the discontinuous tectonics recorded in the course of the study belong to the post-mining stages.
In general, cracks and fractures of the submeridional direction prevail.
On the area of the deposit and its flanks, manifestations of both contact and regional metamorphism are recorded. In the central part of the area, contact metamorphism is manifested in the form of a zone of horn-like rocks with a width of up to 80-100 m and a halo of biotitisation in the frame of the Pistalinsky stock. In the east of
the search area, the western end of the contact halo associated with the Temirkabuk and probably hidden Kulkuduk granitoid massif is recorded.
Metamorphic biotite, concentrated near the exits of intrusive bodies, also covers the entire area of the development of rocks of the Taskazgan formation in the form of scattered inclusions. The rocks of the Taskazgan formation in the field and beyond are metamorphosed at the level of the green shale facies of regional metamorphism.
The degree of metamorphic transformation decreases in the east direction. Characteristic of the metamorphic rocks of the Taskazgan formation is the presence of newly formed albite in an amount of up to 25-30 %, which exceeds the amount of primary clastic feldspar. The chemical composition of the rocks of the formation is characterized by an increased content of Na2O (and in general alkalis) and is close to granitoids.
The above mentioned may indicate the manifestation of sodium metasomatosis in the rocks of the area. From the surface, most of the area of the deposit is covered by quaternary deluvial-proluvial deposits (loam, sand-gravel-gravel material). The thickness of quaternary deposits varies from a few meters in the southern part of the deposit, to 1040 m in the northern part [30].
CONCLUSION
Gold mineralization is located in albite-quartz-muscovite metasomatites developed along the zones of shale formation of the host rocks. The deposit contains 11 closely related ore deposits (ore deposits 1, 1a, 2, 2a, 3, 3a, 3b, 4, 5, 6, and 7), represented by linearly elongated mineralized zones that are sub-consistent with the host rocks. In the northern part of the deposit, the ore deposits have a north-eastern strike, in the southern - a submeridional strike. The fall of the deposits mainly to the north-west at an angle of 30 to 50-600. They are traced from 220 to 840 m along the strike, and 110390 m along the fall.
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