Candle machine

1.

Fujiawu copper deposit is one of the important deposits in Dexing porphyry copper deposit, which is located in the southeast end of the ore field. Its geotectonic unit, strata and structure of the mining area are the same as those of Tongchang and cinnabar red, which will not be repeated in this section

The intrusive rock is trapezoidal on the surface, 650m long in NE direction and 300m wide in NW direction, with an area of 0.2km < sup > 2 < / sup > (Fig. 2-34). The rock mass is trending nw310 ° The side angle is 40 ° about. The horizontal cross-sectional area of the rock mass increases by 0.8km < sup > 2 < / sup > at the elevation of - 200m, and the direction of the long axis of the cross-section of the rock mass also changes from NE to NW. The boundary of the rock mass is relatively straight with few lateral branches

the main rock body and surrounding rock are in intrusive contact, and the contact boundary is clear, showing a mutation relationship. In some sections, there are contact breccias several meters wide, which are mainly composed of wall rocks

the main rock mass causes a certain degree of contact metamorphism to the light metamorphic surrounding rock, and the metamorphic degree of footwall is usually higher than that of hanging wall. According to the degree of metamorphism, it can be divided into two zones: the inner zone is hornblende zone and the outer zone is spotted phyllite zone

Fig.2-34 geological map of Fujiawu copper deposit; 2 - the second lithologic member of Jiu formation of pre Sinian system; 3 - the first lithologic member of Jiu formation of pre Sinian system; 4 - chlorite (epidote) - hydromica phyllite (metatuff); 5-chlorite (epidote) - hydromuscovitization phyllite (metatuff); 6 - quartz hydromuscovitization phyllite (metatuff); 7-6 and 7 were not divided; 8-quartz-hydromuscovitization granodiorite; 9 - chlorite (epidote) - hydromuscovitization granodiorite porphyry; 10 - chlorite (epidote) - hydromica potassic granodiorite porphyry; 11 - quartz diorite porphyrite; 12 - metadiabase; 13 - gabbro pyroxenite; 14 - fine grained felsic; 15 contact breccia; 16 - geological boundary; 17 - schistosity occurrence; 18 - alteration zone boundary; 19 - anticline and its dip direction; 20 - syncline and its plunging direction; 21 - fault; According to geophysical data, Fujiawu, Tongchang and cinnabar red complex porphyry bodies converge into a large concealed rock mass at a depth of 1800m, because Tongchang rock mass has been inserted into the bottom of cinnabar red rock mass more than 800m underground

According to the quantitative statistics (area%) under microscope, quartz varies from 18 to 23, with an average of 20.5; Plagioclase (mainly medium feldspar) varies from 43 to 55 with an average of 48.5; Potash feldspar varies from 13 to 18, with an average of 15.5; Amphibole varies from 7 to 10, with an average of 8.3; Biotite varies from 3 to 7 with an average of 4.8. The composition of the by-ores in the main rock mass of Fujiawu can be divided into (10 < sup > - 6 < / sup >): magnetite varies from 847 to 9674, with an average of 0; Apatite is 130-521 with an average of 351; Sphene ranges from 0.3 to 289, with an average of 145; Zircons range from 13.3 to 255, with an average of 194. The chemical compositions of the rocks are listed in table 2-23 and compared with those of the same kind in China and the world; Table 2-24 shows the CIPW values of Fujiawu porphyry. The main oxide characteristics of the porphyry are reviewed

Table 2-23 petrochemical composition of Fujiawu porphyry rock

Table 2-24 CIPW value of Fujiawu porphyry (W < sub > b < / sub > /%)

SiO < sub > 2 < / sub > content varies from 64.27% to 66.13%, with an average of 65.05%, It is higher than the average value of granodiorite in China and close to the average value of granodiorite in the world. Al < sub > 2 < / sub > o < sub > 3 < / sub > varies from 15.34% to 16.67%, with an average of 15.74%, which is lower than the average of similar rocks in China and the world. Fe < sub > 2 < / sub > o < sub > 3 < / sub > + FeO varies from 3.55% to 4.98%, with an average of 4.20%, which is also lower than the average quality of similar rocks in China and the world. MgO varies from 1.36% to 2.90%, with an average of 1.69%, which is lower than the average of granodiorite in China and the world. Cao varies from 2.89% to 4.66%, with an average of 3.57%, slightly lower than the average of granodiorites in China and the world. Na < sub > 2 < / sub > O + k < sub > 2 < / sub > o varies from 6.37% to 7.65%, with an average of 7.08%, higher than the average of granodiorite in China and the world; In particular, K < sub > 2 < / sub > o content is higher, which constitutes the main characteristics of porphyry petrology

The K-Ar isotopic age of quartz K-feldspar vein in the Fujiawu granodiorite porphyry is 157 Ma, and that of quartz K-feldspar vein in the wall rock of the deposit is 152 ma

(2) ore body: the shape and occurrence characteristics of Fujiawu ore body are shown in table 2-25 and figure 2-35. The central axis of the copper bearing porphyry stock is NW dipping with an angle of 40 °～ twenty ° The ore body at the top of the rock mass has been denuded, and the ore body in the contact zone around the upper part of the rock stock is well preserved, so the shape of the ore body is a hollow cylinder inclined to the northwest, and the horizontal section is circular. The enrichment center of Cu Mo mineralization coincides with the structural faults and fracture intensive zones in the outer inner contact zone. The intensity of copper mineralization is roughly symmetrical with the contact zone, and a single copper ore body is distributed in the deep part of the deposit, especially in most of the contact zone of porphyry. The continuity of mineralization in the main ore body is very good, and there are few inclusions

Table 2-25 morphological features and occurrence of ore bodies in Fujiawu copper deposit; 2-granodiorite porphyry

ore minerals: the ore minerals of Fujiawu are basically similar to those of Tongchang, which can be described in the section of Tongchang, and will not be repeated in this section. The distribution of main metal sulfides in the ore is as follows: Pyrite 3.30%, chalrite 1.39%, chalcocite 0.053%. The ratio of pyrite: chalrite: molybdenite is 2.4:1:0.038. Chalrite accounts for more than 90% of copper minerals, followed by bornite, tetrahedrite and chalcocite

ore structure: it is basically similar to that of copper plant, and will not be repeated in this section

ore reserves, grade and chemical composition: the Fujiawu deposit has 2.5726 million tons of copper reserves with a copper grade of 0.501%; The molybdenum reserve is 167845t and the molybdenum grade is 0.033%; The contents of associated gold, cobalt and selenium are 0.055g/t, 0.0024% and 0.0015%, respectively. Primary ores are dominated by primary copper sulfide, which usually accounts for about 90% of copper reserves. Secondary copper sulfide accounts for 5% ~ 10%, and copper oxide and copper sulfate account for less than 5%. In addition to copper, there are copper, gold, silver, rhenium, nickel, cobalt, sulfur, selenium, tellurium, titanium, potassium, platinum group elements, etc. The main harmful impurity elements in ore are as, Zn, Mg, etc. The average content of arsenic is 0.007%, the content of zinc is usually less than 0.01%, and the content of magnesium oxide is generally less than 2%

The wall rock alteration of Fujiawu deposit is basically similar to that of Tongchang, but the altered mineral content is different. Therefore, table 2-26 can be compared with that of Tongchang

Table 2-26 mineral content of rock in alteration zones of Fujiawu porphyry type Cu (MO) deposit × 10 < sup > - 6 < / sup >; Other contents in%

the alteration process of Fujiawu deposit is explained as follows:

potassium silicate alteration: it mainly occurs in the form of quartz potassium feldspar vein. The measured K-Ar isotopic age of potassium feldspar vein is 152-157ma, which is very short from 163ma of granodiorite porphyry, indicating that potassium silicate alteration was formed with the late stage of porphyry magma, It is the result of the metasomatic reaction between the late independent fluid phase of porphyry magma and the crystallized porphyry and adjacent country rocks. Potassium silicate alteration procts are mainly potash feldspar, followed by biotite, anhydrite and albite

quartz sericite chloritization: the K-Ar isotopic age of the altered sericite is 112 Ma, and the granodiorite porphyry has been crystallized for a long time. During this period, the tectonic movement caused the occurrence of dense fracture zone in the upper porphyry contact zone, but the magma chamber in the lower part continued to discharge alkali rich and volatile fluid, which led to the convection circulation of Tianshui and formed mixed fluid phase. Finally, the rocks (porphyry and phyllite, etc.) around the contact zone were metasomatized mainly by hydrolysis. Hornblende and biotite decompose into sericite and quartz, and iron combines with hydrogen sulfide to form a large amount of pyrite, thus forming quartz sericite chloritization zone

Carbonate sulfation: in the late stage of magma chamber consolidation, there is some resial heat, which drives the convection circulation of Tianshui, and the physical and chemical conditions of thermal fluid slowly recover to the state of crust surface. The alteration formed in this stage is mainly calcite, dolomite, ankerite and gypsum, followed by manganese siderite, fluorite, barite and zeolite

Stable isotope: sulfur isotope composition of sulfide in Fujiawu and nearby sulfur deposits is shown in table 2-27, while sulfur isotope composition of sulfate is shown in table 2-27 δ< Sup > 34 < / sup > s ranges from - 0.6 ‰ to 1.0 ‰, with an average of 0.48 ‰; Sulfur isotope of sulfide in sulfur ore δ< Sup > 34 < / sup > s is 0.5 ‰ - 1.3 ‰, with an average of 0.97 ‰. This shows that sulfur isotope composition of sulfide in Fujiawu and sulfur deposit is homogeneous, which is basically close to meteorite sulfur. Sulfur isotope of Fujiawu sulfate δ< Sup > 34 < / sup > s ranges from 6.1 ‰ to 7.6 ‰, with an average of 7.1 ‰ (table 2-28). This indicates that the sulfur isotopic composition of these sulfates is quite different from that of seawater sulfates. The sulfur source of these sulfates is not from seawater sulfates, but mainly from deep sulfur sources

Table 2-27 sulfur isotopic composition of sulfide in Fujiawu copper deposit- Table 2-30 composition of fluid inclusion in quartz of Fujiawu copper deposit, Table 2-31 composition of elements related to ore forming in fluid inclusion of quartz in Fujiawu copper deposit. Table 2-29 shows the evolution trend of the reaction between porphyry and mixed fluid, and the oxygen isotope composition of granodiorite magma graally evolved into Tianshui

Fluid inclusions the fluid inclusions in the Fujiawu deposit include gas inclusions, multiphase inclusions, gas-liquid inclusions and CO < sub > 2 < / sub > inclusions. The gas-liquid ratio usually varies from 10% to 40%, and a few from 50% to 80%. The main Daughter Minerals of multiphase inclusions are halite, potash and anhydrite. The volume content of CO < sub > 2 < / sub > in CO < sub > 2 < / sub > inclusions varies from 10% to 15%. The diameter of most fluid inclusions varies from 5 to 10 μ m. A few are up to 10 μ It is more than 5 m. Most fluid inclusions are homogeneous in temperature range

2.

Up to now, no special research has been done on the clay minerals formed by hydrothermal fluid alteration in Jinshan gold deposit. Clay minerals (mainly illite and chlorite) were separated from carbonaceous phyllite, altered mylonite, altered ultramylonite and auriferous quartz vein samples to study the genesis and characteristics of clay minerals ring fluid interaction in Jinshan gold deposit

First, the sample was crushed into about 5mm particles and soaked in distilled water for 48h. Then, according to Jackson's (1979) purification method, the carbonate, iron cement and organic matter in the sample were removed with HCl and H < sub > 2 < / sub > o < sub > 2 < / sub > and then extracted from the sample by conventional method μ In order to eliminate the influence of sample thickness on the results of crystallinity determination (Kisch, 1991), clay samples with a thickness of about 3 mg / cm < sup > 2 < / sup > were made into air dried oriented tablets (AD)

(2) X-ray identification of samples the identification of clay minerals was completed by using the D / max RA X-ray diffractometer of modern testing center of Nanjing University. The test conditions of natural air dried sample (AD sheet) and hexanediol treated sample (GL) are Cu target, voltage is 40kV, current is 20mA, step width is 0.01 ° two θ， Scan range 3 °～ thirty-seven °， The content of clay minerals is calculated by using the weight intensity peak of biscaye (1965). The crystallization index of illite is the Kubler index obtained by measuring the FWHM of the 001 (1nm) diffraction peak of illite (Eberl et al., 1989). The diffraction peak intensity ratio (IR) is the srodon peak intensity ratio (srodon et al., 1984) of illite obtained by dividing the ad sheet (I < sub > 003 < / sub > / I < sub > 001 < / sub >) by the GL sheet (I < sub > 003 < / sub > / I < sub > 001 < / sub >). The polytype of illite is derived from clay minerals (< 2 μ m) The test conditions are Cu target, voltage 40kV, current 20mA and step width 0.01 ° two θ， Scanning range 28 °～ thirty-six ° The crystallization index of chlorite is obtained by measuring the FWHM of I < sub > 002 < / sub > (0.7nm) diffraction peak of chlorite. The removal of chlorite from the clay mineral assemblage was carried out by longstaffe (longstaffe, 1986; Ayalon et al., 1988)

The clay minerals in carbonaceous phyllite, Chloritized phyllite and altered rocks in Jinshan Gold Mine μ m) The crystallinity of assemblage, illite, polymorph and chlorite are listed in table 6-1

Table 6-1 clay minerals in altered rocks and carbonaceous phyllite of Jinshan Gold Mine μ m) According to table 6-1, figure 6-1 and figure 6-2, the clay mineral assemblage of all tested rocks is illite + chlorite. Among them, illite is more abundant in mylonite than chlorite, and chlorite is more abundant in ultramylonite than illite. Illite is the main gold bearing quartz vein. Illite in mylonite is more common in 2M < sub > 1 < / sub > than in ultramylonite in 2M < sub > 1 < / sub > and 1m

The crystallinity of illite and chlorite is 0.21-0.24 and 0.25-0.26 respectively. In the clay minerals of Chloritized phyllite, the crystallinity of illite is 0.17, the crystallinity of chlorite is 0.21, and the polytype of illite is 2m < sub > 1 < / sub >

On the whole, the crystallinity of illite and chlorite is 0.16-0.37 and 0.17-0.36, respectively. It can be seen from figure 6-3 that there is no obvious correlation between the crystallinity of illite and that of chlorite. Therefore, it can be considered that the formation and crystallization of illite and chlorite in the process of fluid interaction are not only controlled by temperature and pressure, but also by fluid composition and rock type of surrounding rock

Fig. 6-1 altered mylonite and phyllite clay minerals (< 2 μ m) X-ray diffraction pattern (AD sheet) CHL chlorite; Ill illite; Feld feldspar

Fig. 6-2 altered ultramylonite and gold bearing quartz vein clay minerals (< 2 μ m) X-ray diffraction pattern (AD sheet) CHL chlorite; Ill illite; Q-quartz; Feld feldspar; Cal - calcite; Figure 6-3 crystallinity relationship of illite / chlorite in Jinshan Gold Mine Δ two θ); The illite crystallinity is 0.4-0.21 in the shallow zone or near metamorphic zone (200-370 ℃) Δ two θ); Low grade metamorphic zone (greenschist facies) (> 370 ℃), illite crystallinity less than 0.21 Δ two θ)( Suo Shutian, 1995); The crystallinity of chlorite ranges from 0.21 to 0.28 Δ two θ) According to the analysis, the metamorphism of phyllite and Chloritized phyllite in Jinshan area is greenschist facies, while the metamorphism of altered mylonite and altered ultramylonite in Jinshan gold mine is sub greenschist facies. This indicates that retrograde metamorphism occurred in Jinshan ctile shear zone under the action of fluid

3.

Wang Mou Wang Guo Li Yanlong Zhang Lei Zhu Mingyong Zhang Guanghui

(216 Nuclear Instry Brigade, Urumqi 830011, Xinjiang)

[Abstract] the exploration of Baiyanghe uranium beryllium deposit has made a breakthrough in volcanic uranium polymetallic deposits in Xinjiang after several stages of regional geological survey, pre survey and general survey. Uranium, beryllium and molybdenum ore bodies mainly occur in the contact zone structure of granite porphyry. Beryllium ore bodies have the characteristics of large scale and good continuity. The proved beryllium resources are very large, the uranium ore body is medium, and the molybdenum ore body is small. It is the largest beryllium, uranium and molybdenum ore deposit in China. By summarizing the basic geological characteristics of the deposit, the "Baiyanghe type" metallogenic model and prospecting model are established, which effectively guide the prospecting work of regional uranium polymetallic deposits

[Key words] granite porphyry; Uranium beryllium deposit; Contact zone structure; Baiyanghe uranium beryllium deposit is located in hebukeser Mongolia Autonomous County, Xinjiang, 70km to the East and 25km to the West. It is administratively under the jurisdiction of Hecheng hebukeser Mongolia Autonomous County, with convenient transportation in the mining area

The process of discovery and exploration of Baiyanghe uranium deposit began in 1956 and has a history of more than 50 years. In the 1950s, in the process of uranium prospecting, the former 519 brigade of the Ministry of second machinery found that be had reached the requirements of instrial utilization through semi quantitative spectral analysis. From 1988 to 1989, the 216 brigade of Northwest Geological Exploration Bureau of nuclear instry concted a special study on the existing forms of beryllium and the relationship between uranium and beryllium in Baiyanghe uranium deposit. It is considered that beryllium deposit has a good prospecting prospect. The above work has accumulated valuable geological data and rich prospecting experience for later ore prospecting. Since 2006, the 216 brigade of nuclear instry has studied the previous basic geological data. It is believed that the Yangzhuang fault (f < sub > 1 < / sub >) in the xuemishan volcanic belt is an important rock controlling and ore guiding structure of Baiyanghe deposit, and the contact zone structure of granite porphyry is the main occurrence location of uranium polymetallic ore bodies, Baiyanghe area has the prospecting potential of forming super large beryllium uranium polymetallic deposit. In 2007, China National Bureau of geology of nuclear instry organized experts to carry out on-site investigation and demonstration, and decided to carry out comprehensive prospecting at three levels: one is the 1 ∶ 100000 regional prediction and evaluation of volcanic rock belt, the other is the 1 ∶ 50000 regional geological survey of Yangzhuang rock body and its periphery in Baiyanghe area, and the third is the detailed survey at Baiyanghe No.2 site

From 2008 to 2010, in order to evaluate the metallogenic potential of volcanic type uranium deposits in Baiyanghe area as soon as possible, implement the uranium polymetallic ore procing areas for exploration, and achieve a breakthrough in geological exploration results, the technical idea of "combining comprehensive research with key anatomy, and combining general research with engineering verification" was adopted, The 1 ∶ 50000 regional geological survey of uranium deposit was carried out in Baiyanghe area. Through large spacing drilling verification and intensive dissection of favorable sections, the deep morphology and ore bearing property of Yangzhuang rock body, ASUDA rock body and xiaoyanghe rock body were preliminarily understood, and three favorable metallogenic sections < sup > [2] < / sup > were implemented. The drilling workload was 19000m, 65 drilling holes were drilled, 7 instrial uranium holes and 29 instrial beryllium holes were found. In 2008, a detailed investigation and prospecting work was carried out at the No.2 site of Baiyanghe mining area, and a medium-sized beryllium ore procing area was confirmed

From 2011 to 2013, in order to understand the geological characteristics of the Yanghe deposit, implement the resources of the uranium polymetallic deposit, and provide the basis for further exploration of the deposit, according to the exploration deployment idea of "uranium based and comprehensive prospecting", the general survey was carried out on the 17-136 lines of the Baiyanghe mining area, and the survey was carried out on the ASUDA section Pre prospecting work has been carried out in ARI and lati sections. The amount of drilling work completed is 104000m. According to the general instrial index, the beryllium oxide resource is estimated to be very large, the uranium resource is estimated to be medium, and the molybdenum resource is estimated to be small. The Baiyanghe deposit is the largest beryllium type beryllium uranium molybdenum deposit in China

The Baiyanghe deposit is located in the shaerburti mountain area of West Junggar, and the strata are exposed from old to new in the upper Devonian tarbahatai formation (d < sub > 3 < / sub > t), Carboniferous and bukehe formation (C < sub > 1 < / sub > HB), heihantou formation (C < sub > 1 < / sub > H), Neogene tahihe formation (n < sub > 1 < / sub > t) and Quaternary (q) (Fig. 1)

It is mainly distributed in Yangzhuang rock body γπ P < sub > 1 < / sub >) in the north, southwest and northwest of the deposit, there are continental intermediate acid volcanic rock and pyroclastic rock formation intercalated with normal clastic rock, with an overall dip of 160 °～ one hundred and ninety °， Dip angle 40 °～ sixty °

The lower Carboniferous, bukehe formation and heihantou formation are mainly distributed in the south of the deposit, extending in a nearly East-West trend, with Yangzhuang fault as the boundary

The Neogene Miocene tahihe formation is distributed in the South and northeast corner of the deposit, and its lithology is yellow sandy clay

Quaternary System: it is widely distributed in the East and southeast of the deposit, which is alluvial, proluvial and accumulation

2.2 structure

the Baiyanghe deposit is located in the barrek shaerburti fold belt, between the wuerkashershan anticline saimistai anticline and the Baiyanghe syncline bahali monocline. The NNE trending mengkelake fault and the EW trending degelieti fault are separated on both sides of the deposit, and the nearly EW trending Yangzhuang fault runs through the whole area (Fig. 2). The geological structure is relatively complex, and folds and faults in different directions are relatively developed. Since the late Paleozoic, volcanic activity and magmatic intrusion have been very strong. The rocks of Baiyanghe deposit are mainly acidic volcanic rock formation, intercalated with intermediate basic volcanic rock formation

2.3 intrusive rocks are widely distributed in the Baiyanghe deposit and are obviously controlled by faults. According to the occurrence state of intrusive rocks, they can be divided into meso plutonic intrusive rocks, ultra hypabyssal intrusive rocks and dikes

The intrusive rocks are pyroxene diorite and plagioclase granite

Fig.1 geological sketch of Baiyanghe deposit; 2 - tasihe formation; 3 - the third lithologic member of heihantou formation; 4 - the second lithologic member of heihantou formation; 5 - the first lithologic member of heihantou formation; 6 - upper subgroup of hebukehe formation; 7-the seventh layer of the lower subgroup of hebukehe formation; 8-the sixth layer of upper subgroup of hebukehe formation; 9-the fifth layer of upper sub formation of hebukehe formation; 10 - the fourth layer of upper subgroup of hebukehe formation; 11 - the third layer of upper subgroup of hebukehe formation; 12 - the second layer of the upper subgroup of hebukehe formation; 13 - the first layer of upper subgroup of hebukehe formation; 14 - the fourth lithologic member of talbahatai formation; 15 - the third lithologic member of talbahatai formation; 16 - granite porphyry and its dipping stage number; 17 - the number of granite and intrusive stage; 18 - diorite porphyrite and intrusive stage number; 19 - pyroxene diorite and its intrusive stage number; 20 - diabase; 21 - angular unconformity boundary; 22 - intrusive contact boundary; 23 - fault; 24 - inferred fault; 25 - translational fault; 26 - reverse fault; 27 - normal fault; 28 - uranium mineralization point and No.

ultra hypabyssal intrusive rock is granite porphyry γπ P < sub > 1 < / sub >). The rock mass is nearly East-West beaded, about 10km in length from east to west, and the width from north to South varies greatly, with the widest of 1.8km and the narrowest of 0.1km, covering an area of about 6.9km < sup > 2 < / sup >, and is composed of Yangzhuang rock mass, ASUDA rock mass and xiaoyanghe rock mass (Fig. 3)

Fig. 2 structural sketch of Baiyanghe deposit; 2-neogene red clastic rock formation; 3-acid volcanic rock formation; 4 - intermediate acid volcanic rock formation; 5 - intermediate basic volcanic rock formation; 6-granite; 7-granodiorite; 8-granite porphyry; 9-yanghe deposit range

the northern boundary of Yangzhuang rock body generally inclines to the South (locally to the North) and intrudes into the Devonian System with an dip angle of about 32 ° The southern boundary dips northward with an inclination of 45 °～ seventy-five ° ， It is in fault contact with Carboniferous system (f < sub > 1 < / sub >). Generally, it is thick in the South and thin in the North (Fig. 4)

Ma Hanfeng of Beijing Institute of geology of nuclear instry has measured the formation age of Yangzhuang pluton by whole rock nd SR method, and the age is (293 ± 15) It was formed in Late Carboniferous to early Permian

2.4 dikes

diabase βμ： Most of them intersect in the rock mass in a north-south strike, parallel arrangement, strike 340 °， It is 10-1000m long and 0.5-20m wide. The main component is plagioclase, filled with pyroxene, and the accessory minerals are magnetite (15%), a little hematite and chromite

Fig. 4 North South profile of Yangzhuang rock body

1 - Lower Carboniferous and bukehe formation; 2 - Upper Devonian tarbahatai formation; 3-subvolcanic rock mass; 4-granite porphyry; 5 - diabase; 6 - tuff; 7-tuffaceous siltstone; 8-carbonaceous mudstone; 9-fracture zone; 10 - contact boundary; 11 - borehole location; 12 - Instrial beryllium mineralization; 13 - low grade ore body; 14 - fault

diorite porphyrite δπ： To 340 °， It is 5-15m wide and 400-2500m long. Dark purple microcrystalline diorite porphyry, 20-50cm wide, appears at the edge of the dyke

2.5 hydrogeological characteristics

2.5.1 groundwater types and distribution characteristics

Baiyanghe deposit is located in the South Piedmont hilly area of xuemishan mountain, in the sub area of fracture water of intrusive and eruptive rocks in the hilly plain hydrogeological area (II < sub > 1 < / sub >)

2.5.2 groundwater recharge, runoff and discharge conditions

the climate of Baiyanghe deposit is dry, the humidity coefficient is only 0.057, and the surface water system is rare. The groundwater is only exposed below the local section of the Piedmont. The spring flow is 0.01-0.13l/s, the salinity is 0.5-1.0g/l, and the pH value is 7.0-8.0. The hydrochemical types are so < sub > 4 < / sub > · Cl and so < sub > 4 < / sub >. The groundwater can directly pass through the weathering fissures and structural windows of granite porphyry, tuffaceous pyroclastic rocks and other rocks exposed on the surface, receive the recharge of atmospheric precipitation and pore phreatic water, run off from north to south, and have a certain bearing capacity near the regional ore controlling fault zone. There are three ways of discharge: one is vertical evaporation in arid climate; The second is through the north-south direction of the main ditch of the deposit; No. 1 spring at Dagangou in the eastern part of the deposit is one of the discharge sources of the deposit

2.5.3 aquifer (zone) and its characteristics

according to the lithology, structural structure and water bearing characteristics of rocks, the groundwater along the profile can be divided into: fractured phreatic aquifer (I), fractured aquifer in the hanging wall of contact zone (II) and fractured confined aquifer in the footwall of contact zone (III) (Fig. 5)

Fig. 5 hydrogeological section of line 25 of Baiyanghe deposit

1 - granite porphyry; 2-upper Devonian tarbahatai formation; 3-tuffaceous siltstone; 4-carbonaceous mudstone; 5-granite porphyry; 6 - diabase; 7-fracture zone; 8 - pumping test section and number; 9 - water bearing zone boundary; 10 - number of water bearing zone; 11 - fracture tendency and dip angle; 12 - water bearing zone; 13-phreatic aquifer of aquifuge (I)

stored in granite porphyry γπ P < sub > 1 < / sub >)