Delny mining area is located in the east of Anima Green Fold Belt of Bayan Kara Fold System, on the north side of Anima Green Front Fault, and in the middle of Delny ultrabasic rock body in the east of Anima Green Ultrabasic Rock Belt (Figure 2-24). Anima Green Fold Belt is a rift system.
Figure 2-24 Regional Geological Schematic Diagram of dur' ngoi Region in Delny Region.
R- tertiary red glutenite and mudstone; 1-Cretaceous purplish red conglomerate, glutenite and sandstone; 2- Middle and Lower Jurassic coal-bearing clastic rocks; 3- Upper Permian limestone mixed with sandstone; 4— Metamorphic sandstone and slate with limestone in the upper part of Lower Permian; 5-Lower Permian slate and metamorphic sandstone mixed with volcanic rocks; 6- Upper Carboniferous crystalline limestone and marble amphibole; 7- granite; 8- syenite; 9- diorite; 10-ultrabasic rock; 1 1- geological boundary; 12- sedimentary unconformity line; 13-measured and inferred reverse fault; 14- measured and inferred faults with unknown properties; 15- structural fracture zone; 16- Delny mining area
Second, the regional geology
(1) stratigraphic survey
Upper Paleozoic is the main stratum in this area, followed by Middle and Lower Jurassic, Cretaceous, Tertiary and Quaternary. From the old to the new, briefly described as follows:
Upper Carboniferous (C2): outcropped in the middle of this area, with northwest-southeast distribution. It is divided into four layers: amphibolite mixed with marble, marble, biological limestone and crystalline limestone. There is a gradual relationship between classes. Biolimestone is rich in brachiopod fossils, and the stratigraphic age is Upper Carboniferous. The K-Ar age of amphibole in the north of Delny River Basin is 742Ma. 199 1 year, the Rb-Sr isochron ages of amphibolite and marble in the north of the mining area of 203Ma were measured by Northwest Institute of Nonferrous Geology, indicating that Neoproterozoic tectonic debris exists in the rocks in this area.
Permian (P): This area is widely distributed, mainly in the southern half.
Lower Permian (): mainly composed of slate and metamorphic sandstone, with metamorphic volcanic lens.
Upper Formation of Lower Permian (): mainly exposed in the south of this area, extending in a belt shape in the northwest direction, consisting of metamorphic sandstone, slate and limestone, and occasionally metamorphic volcanic rocks, constituting the sedimentary formation of flysch-like rocks. Limestone is rich in fossils.
Upper Permian (P2): mainly exposed in the middle of this area, composed of limestone and sandstone.
Middle-Lower Jurassic (J 1-2): It is distributed at the eastern end of the region and consists of a set of coal-bearing clastic rocks, mainly sandstone, sandy shale and shale, with conglomerate at the bottom. This set of rocks belongs to continental lake basin deposits.
Cretaceous (K): distributed in the northern half of this area, it is a set of purple conglomerate, glutenite and sandstone.
Tertiary (R): It is exposed in the middle of the region and consists of a set of red conglomerate, glutenite and mudstone.
(2) Regional magmatic activity
Ultrabasic rocks are distributed intermittently for about 300 kilometers along Jishishan and Anima Qing Mountains, forming the "Jishishan Ultrabasic Rock Belt". Known as "Anima Qingshan ultrabasic rock belt" in Qinghai, it is generally NW-trending or NWW-trending. Acid intrusive rocks are distributed in the north side of the rock belt, and ultrabasic rocks are distributed in the south side of the rock belt. And ultrabasic rocks are dominant. These intrusive rocks are often concentrated with fault structures, forming a fault intrusive rock belt with a width of about 3 ~ 5 km.
1. ultrabasic intrusive rocks
The "Animaqingshan ultrabasic rock belt" consists of a series of rock masses with different sizes, which are parallel or connected with each other. The largest rock mass is the Delny ore-bearing rock mass, with the length of 17km and the widest point of1000 m. Small rock mass is only a few meters to tens of meters long.
The ultrabasic rocks are mainly plagioclase pyroxenite, followed by peridotite, dunite, pyroxenite and a small amount of gabbro. All the rocks except gabbro have become serpentine. The rock composition is mainly composed of chrysotile, serpentine, collophanite and sericite, with residual crystals of orthopyroxene locally, and various sulfides, magnetite and spinel in the rock.
Almost all ultrabasic rocks occur in the lower strata of Lower Permian, and a few occur in Upper Carboniferous or Upper Permian. On the plane, the rock mass is irregular strip, mostly along the bedding occurrence, and changes with the change of stratum occurrence. Generally, there is no contact metamorphic zone with surrounding rock, and sometimes mixed dyeing can be seen.
This ultrabasic rock was originally defined as the intrusive product of late Variscan. In recent years, two new viewpoints have been put forward. First, the ultrabasic rock belongs to the Paleoproterozoic (Pt 1-2) volcanic peridotite series, and the Sm-Nb isochron age of ultrabasic rock and basalt series is 1027 Ma, and the Rb-Sr isochron age is 672Ma. Another view holds that the Qingshan ultrabasic rock belt in Anima belongs to ophiolite assemblage.
2. Acid intrusive rocks
It is distributed in the northern part of ultrabasic rock belt, and large and small rock masses are densely exposed, which constitutes the acidic intrusive rock belt in this area. The lithology is mainly granite, and the rest are granodiorite, amphibole granite, granite syenite, syenite and diorite. These rocks are all in the form of small rocks, and the scale is very small.
Granite is dominated by biotite granite, with fragmented granite locally, and gneiss structure is extremely developed, especially near the mining area. The era is Yanshan period. However, some people think that it is mixed granite, which is the product of old structural fragments.
3. Volcanic rocks
Volcanic rocks in this area are distributed in Permian, which are basalt and basaltic andesite, and tuff is occasionally seen. Metamorphic andesite occurs along the stratum, with discontinuous lenticular distribution. At the contact point between andesite and slate, its composition changes gradually, which is formed by underwater eruption.
(C) the basic characteristics of regional structure
The whole regional tectonic line is NW-trending. The long axis direction, fold axis direction and fault zone direction of rock mass are roughly the same, ranging from 300 to 330. It happened under the action of a group of NE-SW compressive stresses with long-term activity and inheritance.
The mainland with the Qaidam block as the core already existed in Paleoproterozoic, and the area around Animaqingshan was the result of the spread of the ancient Qaidam land in Mesoproterozoic and Neoproterozoic. Basalt in this zone is the product of active continental margin and belongs to the ancient land on the northern margin of Qaidam basin. In the Late Paleozoic, the Qingkunnan-Maqin fault and the Buqingshan-Jiang Qian fault in Anima moved again, forming the Carboniferous-Early Permian active aulacogen, which is active in the deep, with typical island arc type and active continental margin environment, and the rocks have the characteristics of ophiolite assemblage. At the end of Permian, it returned to the closed land. A large-scale Tethys Sea deposit occurred in Triassic, which was blocked by Animaqing Mountain, forming two distinct Tethys Sea areas in the north and south. The vicinity of Buqingshan-Jiang Qian fault is characterized by "mixed accumulation". Since Jurassic, this area has been characterized by continental rift deposits, mainly manifested by upward compression and erosion, forming a series of nappe structures, accompanied by multiple activities of intermediate-acid intrusive rocks.
(4) Aeromagnetic characteristics of regional geophysics.
Aeromagnetic anomalies in this area are distributed in the Jishishan fault-ultrabasic rock belt and Qingshan fault-ultrabasic rock belt in Anima. The distribution length is 150km. There are five main anomalies, the major axis is 3 ~ 25 km, the minor axis is 1.5 ~ 15 km, and the central magnetic field intensity is 30 ~ 170 nt.
The center of 1369 anomaly is Delny copper mine area, and the key geological body causing the anomaly is ultrabasic rock belt. The F 18 fault controls the distribution of the colluvium-Dernish-ultrabasic rocks.
Three. Geological characteristics of the deposit
(1) strata and rocks in the mining area
Delny copper-cobalt deposit is located in the middle of Jishishan ultrabasic rock belt, and the exposed strata in the mining area are Upper Carboniferous (C2) and Lower Permian. Ultra-basic rocks outcrop through the whole mining area, occupying most of the mining area (Figure 2-25).
Figure 2-25 Geological Schematic Diagram of Delny Copper Deposit
α metamorphic andesite; Barium-tuffaceous slate; μ-siliceous rocks; γ-granite; γ δ-granodiorite; φ-ultrabasic rocks, mainly pyroxenite, generally serpentine and carbonate; φsic- silicified carbonate serpentine; φJC- carbonate breccia serpentine: φ с-carbonate serpentine; φ φφse—- flaky serpentine; T-shaped iron hat; 1-Thousands of carbonaceous slates and phyllites in the Lower Permian, mixed with sandstone, metamorphic glutenite and occasionally metamorphic volcanic rocks; 2-C3 Upper Carboniferous marble, crystalline limestone and amphibole; 3- presumption of normal fault; 4- Inferring the reverse fault; 5-measured and inferred translational faults; 6— Faults of unknown nature measured and inferred; 7— Formation occurrence; 8- foliation occurrence; 9— Horizontal projection boundary of ore body
The northern part of the rock mass consists of marble amphibole of Upper Carboniferous and sandstone, carbonaceous slate, phyllite with calcareous slate and siliceous rock of Lower Permian. In the south of the rock mass are thousands of slates of the Lower Permian, among which there are basalt and basaltic andesite lenses.
The length of Delny rock mass group is 17km, which can be divided into three rock zones: north, middle and south. Delny mining area is located at the widest part of the middle rock zone, with a width of about 800m, and its two ends gradually narrow, and there is Zhabenggou North ore zone at the west end. The southern rock belt is on the south side of the mining area and extends to Zhabenggou area. There is the southern mine belt of Zhabenggou on the surface. The northern rock belt is intermittently exposed on a small scale, and there is a mineralization point in Yuanchi Mountain at the western end. Generally speaking, the three rock belts converge to the west and spread to the east. The surrounding rocks of the middle rock belt and the south rock belt are sandstone, millstone slate, carbonaceous slate and basalt of the Lower Permian. The remains of general surrounding rocks exist in the rock mass. There are migmatized cataclastic granite mounds in the northern margin of the middle rock belt. In addition to the Lower Permian, the surrounding rocks of the northern rock belt also include the Upper Carboniferous. The occurrence of ultrabasic rock body changes synchronously with the occurrence of surrounding rock and blends with surrounding rock. The rock mass is mainly pyroxenite, followed by peridotite, with a small amount of dunite, peridotite and pyroxenite. Rock mass is generally serpentine, and olivine can hardly be seen under microscope. Pyroxene is sericitized, and only the residual crystals of pyroxene can be seen. The rock type belongs to magnesium ultrabasic rock, and the average ratio of magnesium to iron is 9.6, belonging to normal series and aluminum supersaturation series. The content of Fe2O3 is higher than FeO, and the oxidation degree is high.
(2) Mining area structure
The mining area is located in the south wing of anticlinorium, Delny, near the mine.
Fold structure: There are many folds in surrounding rock and rock mass, and the axial direction is northwest, which is consistent with the strike of strata and rock mass. The center of the rock mass is consistent with the anticline. There is a syncline on the north and south sides of the anticline. Ore body I is located in the axis of anticline, ore body II is located in the axis of south syncline, and ore body VII is located in the north wing of anticline.
Fault structure: The fault structure in the mining area is dominated by longitudinal faults, while the transverse and oblique faults are undeveloped. Longitudinal faults include reverse fault zone, schist zone and breccia zone.
(3) characteristics of ore bodies
Ore bodies: There are mainly four ore bodies I, II, V and VII in the mining area (Table 2- 10), and 22 small ore bodies, all of which are in ultrabasic rocks, almost all of which are shallow-buried concealed minerals, lenticular or layered, with clear boundaries with surrounding rocks, but obvious folds. Generally, each ore body is thick in the middle and gradually thinner at both ends. Although the ore body occurs in the middle of ultrabasic rock body, the direct roof rock of the ore body in some areas is slate shear sandstone layer with small thickness (Figure 2-26).
Table 2- 10 List of Number, Scale and Content of Main Orebodies Table 2- 10 List of Scale, Grade and Ore Reserves of Main Orebodies
See table 2- 1 1 for the mineral composition of the ore.
Table 2- 1 1 Mineral composition of various ores Table 2-1/mineral content of ores
Fig. 2-26 Cross-sectional view of ore body 1 in Wuer Ngoy Copper Mine, Delny.
1-Quaternary residual. 2-Slate; 3- serpentine; 4- carbonized breccia serpentine; 5- Mineralized flake serpentine; 6- copper-zinc-cobalt-sulfur ore; 7- copper-zinc-sulfur ore; 8- copper-iron-sulfur ore; 9- copper-sulfur ore; 10- copper-sulfur (temporarily difficult to use) ore; 1 1- cobalt-sulfur ore; 12- copper ore (oxide ore); 13-copper ore (temporarily used for oxide ore); 14-stone inclusion; 15-iron cap; 16- ore body boundary line; 17- boundary line of ore industry type; 18- geological boundary; 19- failure; 1- Number of main ore body and small ore body
The main components in the ore: copper, zinc, cobalt and sulfur can be separated from the ore body. Copper content is about 1%, and some samples are as high as 10%. The zinc content is about 65438 0%, and the individual samples are as high as 7.28%. Cobalt content is 0.08% ~ 0. 1%, and individual samples reach 0.4%. Cobalt is mainly dispersed in pyrite and pyrrhotite. Pyrite has the highest cobalt content, followed by pyrrhotite; The cobalt content of pyrite is the highest in the early stage. The sulfur content is generally 30% ~ 40%, and some samples contain 50% sulfur.
Associated components: The associated components with high content in each main ore body are gold, silver, selenium, cadmium, gallium and indium. The content of gold and silver in oxidized ore is higher than that in primary ore. The ore also contains trace thorium and uranium.
See table 2- 12 for ore structure.
Ore type: mostly primary ore, with a small amount of oxidized ore on local surface. The primary ore is massive and banded copper-bearing pyrite ore, which constitutes the main part of the ore body and is mainly distributed in the upper part of the ore body. The banded copper-bearing pyrite ore is mainly distributed in the lower half of the ore body and the pinch-out parts at both ends of the ore body. Disseminated and breccia ores are not widely distributed. Copper-zinc-cobalt-sulfur ore, copper-zinc-sulfur ore and copper-cobalt-sulfur ore are the main types of ore industry.
Distribution law of main components: copper, cobalt and sulfur are basically distributed in the whole ore body, and zinc is mainly distributed in the upper part of the ore body.
(4) Wall rock alteration
Carbonation and serpentine are the most developed and widely distributed wall rock alteration of ore bodies, which are closely related to the space of ore bodies. Followed by slip petrochemical, chloritization, sodium flash petrochemical, silicification, epidote, flash petrochemical, biotite, phlogopite, garnet and so on. These alterations are weak, uncommon and not closely related to ore bodies.
Table 2- 12 Classification of Ore Structures and Structures Table 2- 12 Ore Structures and Structures
Carbonation: Carbonation is widely developed in ultrabasic rocks, and altered minerals include calcite, dolomite and magnesite.
Serpentine fossilization: Serpentine fossilization covers almost the whole ultrabasic rock body, forming a serpentine encirclement with a width of about tens to hundreds of meters around the ore body, and the inner ring is carbonate serpentine. Altered minerals are mainly chrysotile, serpentine and collophanite. There are three stages in the formation of serpentine in ultrabasic rocks, and the second stage is related to mineralization.
(5) Mineralization
1. Geological structure background
The main features of Buqingshan-Animaqing mountain belt are:
(1) It can be clearly seen from the satellite photos that there is a large regional fault in Xiugou-Maqin area on the north side of Anima Green Belt, and the regional gravity and aeromagnetism also show the characteristics of deep fault. This fault is an inherited, long-term deep fault zone and a transitional zone between Tachai ancient land (or North China ancient land) and South China ancient land. Mesoproterozoic has the evolution history of the ancient land margin of North China, and Paleozoic and later have the characteristics of the ancient land of South China.
(2) The upper Paleozoic strata are dominant in the area, with deep rock metamorphism, and phyllite, metamorphic sandstone, marble and even schist and gneiss generally appear.
(3) The isotopic ages of the intermediate-acid intrusive rocks in northern Delny are 120Ma, 153Ma and 174Ma, which belong to Yanshanian, and may include Indosinian and Himalayan rocks. Some fractured granites on the north side of Delny pluton are mixed granites.
(4) The basic and ultrabasic rock belts extend in the NW or NWW direction, distributed intermittently for more than 300 kilometers, and appear in groups. The rock mass is banded, densely arranged in parallel and extending intermittently. There are also paleotectonic fragments exposed in the rock belts of the Middle Ages and Proterozoic. The K-Ar age of amphiboles in northern Delny mining area is 742Ma, the Sm-Nd age of ultrabasic rocks and basalts in Delny area is 1027 Ma, and the Rb-Sr age is 672Ma.
2. Genesis of ultrabasic rocks
With the strengthening of geological research, the understanding of ultrabasic rocks is also deepening.
(1) According to the drilling data, ultrabasic rocks still exist at the depth of 1000 m, and there are copper ore bodies or veins.
(2) The ultrabasic rocks in Delny mining area occur directly in slate, but there is no direct contact between the intermediate volcanic interlayer and ultrabasic rocks, and there is no transitional relationship between them. Basalt in Zhabenggou area is in integral contact with ultrabasic rocks without alteration, and basaltic pyroclastic rocks have siliceous rocks. The massive copper-bearing pyrite in Xishan, Chi Yuan occurs in basalt, while basalt occurs in ultrabasic rocks in small packets.
(3) Generally, contact metamorphism is not seen when the rock mass contacts the surrounding rock, and there are occasional small-scale flaky serpentine at the contact point, which is only a sign of structural contact.
(4) The morphology, occurrence and genesis of "breccia" ultrabasic rocks are complex. One is linear distribution, serpentine is broken into breccia, cemented by carbonate, calcite is reticulate vein, which may be formed by structural extrusion in the late stage of in-situ crushing; The second is the gradual transition between breccia and massive snake mosquito rock. The breccia and cement of breccia serpentine are ultrabasic rock materials, and the size of breccia varies greatly, especially in Zhabenggou section. The distribution of breccia ultrabasic rocks is generally oval, which may have the nature of cryptoexplosion; The third kind of breccia and cement are rocks containing ultrabasic rocks, which are linear or long-axis lenticular. The proportion of cementation components is low and the angle of breccia is vague, which may be self-breaking breccia in ultrabasic rock flow.
(5) There are interwoven spines, comb-like microstructures and flame-like structures in ultrabasic rocks in Delny mining area and its periphery, which indicates that Komati olive lava flow exists in this mining area (Northwest Institute of Nonferrous Geology, 199 1 year).
(6) ultrabasic rocks and surrounding rocks are formed at the same time.
The ultrabasic rocks in the Buqingshan-Qingshan rock belt in Anima were formed in two eras: there were ultrabasic rocks with volcanic jet characteristics in the Middle and Late Proterozoic, and the early Permian was the main period for the formation of ultrabasic rocks in this belt, forming intrusive ultrabasic rocks, which were not far from volcanic sedimentary strata.
3. Metallogenic conditions
The mineralization of (1) Delny deposit is controlled by ultrabasic rock mass, and the size of rock mass has a certain relationship with mineralization. Generally speaking, the larger the rock mass, the better the mineralization, but it is not absolute.
(2) The ultrabasic rocks are controlled by sandstone strata, and the formation time is similar. Moreover, the more interlayer of volcanic rocks in the middle, the greater the possibility of mineralization of ultrabasic rocks nearby.
(3) The distribution of ultrabasic rocks is consistent with the fault zone, in other words, it is also consistent with the distribution of ore zones.
(4) There are many surrounding rock inclusions in ultrabasic rocks, and the long axis direction of the inclusions is consistent with the regional tectonic direction. Some surrounding rock inclusions are obviously syncline structures, and there is a possibility of ore formation in the axis of syncline.
(5) In the whole rock zone, if intermediate-acid intrusive rocks are exposed near ultrabasic rocks, the ultrabasic rocks show mineralization, indicating that there is a certain connection between them in mineralization.
(6) Ultrabasic rocks can be roughly divided into three rock zones. If the rock belts are close to each other, or the rock belts expand and contract, mineralization or industrial ore bodies will appear in the parts where the occurrence changes.
(7) There are eruptive and intrusive ultrabasic rocks in ultrabasic rocks (it is difficult to distinguish them in practice), which is beneficial to mineralization.
(8) There are massive dark green fiber serpentine near the light green serpentine (sometimes in sheet form), and mineralization exists in the latter or the transition between them.
Four. Genesis of ore deposit
General characteristics of (1) deposit
The surrounding rocks of (1) orebody are mainly breccia serpentine, dark green serpentine and diorite dolomite, with carbonaceous tuff locally. The latter often appears in the upper wall of ore bodies.
(2) The boundary between ore body and surrounding rock is clear. There are disseminated mineralization (pyrite and chalcopyrite) around the ore body, and the thickness varies from several centimeters to several meters. In western Delny or Zhabenggou, there are massive vein-like ore bodies with a thickness of 1 ~ 2m on the surface, which are located in disseminated ore zones.
(3) There are 34 ore bodies in the mining area, and each group has a main ore body with several small ore bodies.
(4) The ore bodies are layered, lenticular and goose-shaped, with three horizons, and each ore body is connected end to end.
(5) The ore body and surrounding rock (slate) have synchronous folds.
(6) The middle and upper part of the main ore body is copper-bearing chalcopyrite, and the lower part is copper-bearing pyrrhotite. Composition of metallic minerals: pyrite 80% ~ 90%, pyrrhotite 5%, magnetite 2%, chalcopyrite 1% ~ 2%, sphalerite 0.5% ~ 2%. Dense massive pyrrhotite ore was found in the west of Delny, of which 70% ~ 80% was pyrrhotite, 20% ~ 330% was pyrite, and a very small amount was chalcopyrite and sphalerite.
(7) Carbonate (calcite and dolomite, a little magnesite) and timely are the main nonmetallic minerals in the ore. The former content is below 20%, and the timely content is below 3%. Carbonate and calcite appear irregularly with metal minerals, and some appear in veins. The mineral composition of ultrabasic rocks is generally not found in ores.
(8) Stacked structure, massive structure and banded structure are the main ore structures. The disseminated structures are developed in the edge, periphery and pinch-out parts of ore bodies, as well as in the attached small ore bodies. Breccia structures are widely distributed in ores without obvious regularity.
(9) Carbonization and serpentine are the main wall rock alteration. There is carbonization on the upper wall of the ore body, but no floor is seen. The roof and floor of ore bodies generally have flaky or broken serpentine belts. These two kinds of alteration only have spatial relationship with ore bodies.
(2) Sources of ore-forming materials
(1) Orebodies occur in ultrabasic rocks, and star-shaped sulfides can be found everywhere in all kinds of rocks, especially pyrite.
(2) The average abundance of copper in ultrabasic rocks is only 1/3 of that in the crust, and that of cobalt is less than 1/2, and that of zinc is lower than that in the crust. It shows that the original magma is well differentiated and the ore-forming fluid is rich in copper, zinc and cobalt.
(3) REE patterns of rocks and ores indicate that ultrabasic rocks are products of low melting of mantle, and disseminated ores and massive ores are products of homologous differentiation. Rocks and ores are generated under the condition of relative oxidation. Ores show positive δEu anomalies, while rocks show weak negative anomalies. Basalt and ultrabasic rocks are homologous rather than directly related.
(4) The sulfur isotope δ34S of the ore is -6. 15 ‰ ~ 6.64 ‰ (12), with an average of 6.88‰. 199 1 year data δ34S is -4.32 ‰ ~+8.89 ‰ (1 1 piece). The variation range is small, slightly larger than that of meteorite sulfur. It can be considered that the sulfur source mainly comes from the upper mantle and is mixed with some crustal sulfur.
(5) The initial neodymium of ultrabasic rocks is 0.5 10899, which is close to the initial value of mantle rocks. The δ 18O of ore magnetite is 0.52 ‰ ~ 7.85 ‰, with an average of 4.42‰( 13 block); Magnetite in rocks is 2.41‰; The δ 18O of the whole rock is 5.71‰ ~10.82 ‰ (13), with an average value of 8.37‰, which is higher than that of ordinary ultrabasic rocks. It shows that it belongs to the magma source area and is mixed with foreign materials.
(6) According to the calculation results of a few sulfur and oxygen isotope geological thermometers, the diagenetic temperature of serpentine is1412 ~1496℃, and the sulfide formation temperature is greater than 320℃. The formation temperature of a single pyrite is 2 10℃ (Duan Guolian, 199 1).
(3) Several different views on the genesis of the deposit.
At present, there are different views on the genesis of Delny deposit. Generally speaking, there are the following viewpoints: hydrothermal deposit, sedimentary deposit or eruption-sedimentary deposit, melting-detachment penetration or melting-detachment penetration-hydrothermal deposit, "Delny-style" copper deposit, composite deposit and binary deposit, which have the dual characteristics of magmatic deposit and jet-sedimentary deposit.