Pomegranate cloud computing power

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3.

3.4.1-1, with flake granular meta crystalline structure and gneissic structure. The rocks are composed of garnet (3%) ±、 Muscovite (5% ±、 Biotite (12% ±、 Plagioclase (35% ± And quartz (45% ± The whole has a certain directionality and dense distribution. two ×， Single polarization (left) and orthogonal polarization (right)

3.4.1-2 quartz: heteromorphic granular, colorless, with normal protuberance, wavy extinction, a small amount of granulation elongated mosaic growth, along the direction of foliation, lenticular, banded distribution, particle size 0.3 ~ 2.0 mm, a small amount of & lt; 0.3mm ten ×， Orthogonally polarized light (left); two ×， Orthogonally polarized garnet (right)

3.4.1-3: heteromorphic irregular granular, colorless, extremely high positive protuberance, with irregular cracks, fully extinction under orthographic microscope, weak chloritization, particle size 0.3-1.0 mm, scattered distribution. ten ×， Muscovite: flake, scaly, colorless, with a group of extremely complete cleavage, bright interference color, sheet diameter & lt; 1.5mm, all associated with biotite, banded distribution. ten ×， Single polarization (left) and orthogonal polarization (right)

3.4.1-5 biotite: flaky, scaly, brown light green yellow polychromatic, with a group of very complete cleavage, sheet size & lt; 2.0 mm, strongly Chloritized and weakly MUSCOVITIZED, distributed along the gneissic direction in strips. ten ×， Monoclinic (left) and orthogonally polarized (right)

3.4.1-6 plagioclase: subhedral heteromorphic plate columnar, plate granular, acid plagioclase with fine and dense flake twin crystals, strong sericitization, kaolinite and other clay mineralization, particle size 0.52.0 mm. ten ×， Orthogonal polarization

4.

The granulites of the DACAO Shachang migmatized supracrustal series generally contain subdiopside or perilla pyroxene or two kinds of pyroxene, but rarely contain pyroxene. Garnets are often found in these rocks, some of which belong to epigenetic garnets and contain resial crystals of metasomatized minerals (plate III-1)

Fig. 2-9 w < sub > Ti < / sub > - W < sub > Zr < / sub > diagram of basic metamorphic rocks (according to Pearce, 1982)

WPB intraplate basalt; IAB island arc basalt; MORB mid ocean ridge basalt; 1. Samples of DACAO Shachang migmatized supracrustal series; 2. Samples from the Weiziyu tTG (a) - M-Me complex and yangpodi ttg-m-me complex; 3-sihetang migmatized supracrustal rocks. The sample serial numbers are the same as those in table 2-4

Fig. 2-10, and the illustrations of W < sub > Zr < / sub > / W < sub > y < / sub > - W < sub > Zr < / sub > are the same as those in Fig. 2-9; The sample number is the same as that in table 2-4

Fig. 2-11 1 / 100 · w < sub > Ti < / sub > - W < sub > Zr < / sub > - 3W < sub > y < / sub > diagram of basic metamorphic rocks

a-low-k tholeiite (LKT); B-ocean floor basalt (OFB); C-calc alkaline basalt (CAB); D-intraplate basalt (WPB). The legend is the same as figure 2-9; The sample serial number is the same as that in table 2-4

Fig. 2-12 1 / 3 · w < sub > HF < / sub > - W < sub > th < / sub > - W < sub > TA < / sub > diagram of basic metamorphic rocks

CP convergence plate margin (EA evolution arc; IA - immature arc); MORB mid ocean ridge basalt (n-normal type; E-enriched type); WP - in board. The legend is the same as figure 2-9; The sample number is the same as that in table 2-4

the content of SiO < sub > 2 < / sub > in the seven samples (table 2-6) of this rock group is equivalent to that of neutral intermediate acid transition type, with an average content of 61.86%. In the ACF diagram (Fig. 2-14), two are located in the neutral igneous rock area, and five are located in the overlapping area of neutral igneous rock and greywacke, which is far away from the clay semi clay rock area. In the diagram of W < sub > (CaO + MgO) < / sub > - W < sub > Na < sub > 2 < / sub > o < / sub > / W < sub > k < sub > 2 < / sub > o < / sub > (Fig. 2-15), 4 samples are located in neutral intermediate acid igneous rock area, and 3 samples are located in Archean greywacke area. Based on the above two diagrams, it is inferred that the protoliths of samples 1 and 7 are dacitic volcanic rocks or their tuffs and andesitic volcanic rocks or their tuffs respectively. The protoliths of the other five samples are (tuffaceous) greywacke, which are located in the greywacke area in 1g (W < sub > Na < sub > 2 < / sub > o < / sub > / W < sub > k < sub > 2 < / sub > o < / sub >) - 1g (w < sub > SiO < sub > 2 < / sub > < / sub > / W < sub > al < sub > 2 < / sub > o < sub > 3 < / sub >) (Fig. 2-16). The REE distribution pattern of No. 1 sample is similar to that of Archean fi dacite (Fig. 2-17), and different from that of sandstone and mudstone in different tectonic settings. In the diagram of W < sub > k < sub > 2 < / sub > o < / sub > / W < sub > Na < sub > 2 < / sub > o < / sub > - W < sub > SiO < sub > 2 < / sub > < / sub > (Fig. 2-18), 2 samples are located in the contemporary active continental margin greywacke area, and 3 samples are located in the contemporary oceanic island arc greywacke area; In < inlinemediaobject > < imageobject > < imagedata role = 3 "fileref = image / 037_ Jpg > < title > < title > < title > < title > < Image > < image data > < image image object > < image image Image > < / inline media object > and W < sub > k < sub > k < sub > 2 < / sub > o < / sub > / W < sub > < title > < title > < title > < title > < title > < title > < image image data > < image image object > < image image object > and W < sub > and W < sub > k < sub > k < sub > 2 < / sub sub > 2 < / sub > o < / sub > o < / sub > o < / sub > o < / sub > o < / sub > o < / sub > < sub > < sub > and W < sub > SiO < sub > SiO < sub > SiO < sub < sub > 2 < sub < sub > 2 < sub > < sub > 2 < / sub > < sub > < sub > < sub > 2 < / sub / sub > < sub > < sub > < sub > < sub > < sub > < sub > 2 < / sub > 2 in the diagram of < sub > 3 < / sub > < / sub > / w (CaO + Na < sub > 2 < / sub > o) (Fig. 2-19), It mainly shows the characteristics of contemporary island arc greywacks, and some of them have the characteristics of contemporary active continental margin greywacks

Fig. 2-13 basic metamorphic rocks of < sup > 143 < / sup > nd / < sup > 144 < / sup > Nd - < sup > 147 < / sup > SM / < sup > 144 < / sup > nd diagram

MORB mid ocean ridge basalt; OIB oceanic island basalt; 1. Basalts from southern Hawaii; 2A Aleutian andesite; 2B Aleutian basalt; 3-andean basalt; 4 - middle basic rocks of tarong; 5 - Archean and Proterozoic sedimentary rocks and metasedimentary rocks in Scotland; 6-archean and Proterozoic complexes of the Canadian Shield; 7-lewis felsic granulite. The sample number is the same as table 2-4

Fig. 2-14 ACF diagram of biotite plagioclase granulite (garnet and pyroxene)

a-quartzite; B - hard sandstone; C-clay rock; D-clay shale; E-shale; F-rhyolite; G-dacite; H-andesite; K-basalt; I - ultrabasic rock area; II - basic rock area; III - marl (dolomite) area; IV - hard sandstone area; V - clay semi clay rock area; VI - high alumina clay rock area; Ⅶ - neutral igneous rock area. The sample serial number is the same as table 2-6

Table 2-6 (garnet, pyroxene) biotite plagioclase granulite type chemical composition (W < sub > b < / sub > /%)

note: rock Name: 1-garnet bearing sub transparent biotite plagioclase granulite; 2 - biotite bearing garnet subdiopside plagioclase granulite; 3-garnet bearing biotite lherzolite plagioclase granulite; 4 - Secondary diopside bearing biotite plagioclase granulite; 5-garnet bearing biotite plagioclase granulite; 6-garnet bearing subdiopside biotite plagioclase granulite; 7-biotite perilla plagioclase granulite

Data sources: 1; 2-6-according to Zhou Hongxun et al. (1980); 7-according to Zhou Shaolin et al. (1993)

Fig. 2-15 (garnet, pyroxene) biotite plagioclase granulites w < sub > (CaO + MgO) < / sub > - W < sub > Na < sub > 2 < / sub > o < / sub > / W < sub > k < sub > 2 < / sub > o < / sub > diagram

a-archean calc alkaline andesite average composition (W < sub > SiO < sub > 2 < / sub > < / sub > = 56.7%); B-the average composition of Archean high-k calc alkaline andesite (W < sub > SiO < sub > 2 < / sub > < / sub > = 58.9%); C-The average composition of Archean island arc andesite (W < sub > SiO < sub > 2 < / sub > < / sub > = 57.3%); D-average composition of modern island arc andesite (W < sub > SiO < sub > 2 < / sub > < / sub > = 57.3%); E-average composition of modern calc alkaline andesite (W < sub > SiO < sub > 2 < / sub > < / sub > = 59.5%); F-average composition of modern high-k calc alkaline andesite (W < sub > SiO < sub > 2 < / sub > < / sub > = 60.2%); G-average composition of modern dacite (W < sub > SiO < sub > 2 < / sub > < / sub > = 64.9%); H-average composition of modern island arc dacite (W < sub > SiO < sub > 2 < / sub > < / sub > = 66.8%); The average composition of i-archean fi dacite (W < sub > SiO < sub > 2 < / sub > < / sub > = 67.1%); J-17 Archean greywacks of Sabah formation in South Africa (W < sub > SiO < sub > 2 < / sub > < / sub > = 66.2%) (condie et al., 1970); K-the average composition of 20 Archean greywacks (W < sub > SiO < sub > 2 < / sub > < / sub > = 63.7%) (Henderson, 1972); L-mixed Archean greywacke (W < sub > SiO < sub > 2 < / sub > < / sub > = 63.3%) (condie, 1976); M-the average composition of 23 Archean greywacks in the South Pass greenstone belt, Wyoming (W < sub > SiO < sub > 2 < / sub > < / sub > = 64.4%) (condie, 1976); N-the average composition of 20 Archean slate (W < sub > SiO < sub > 2 < / sub > < / sub > = 57.8%) (Henderson, 1972); O average composition of slate in Archean greywacke argillaceous pair (W < sub > SiO < sub > 2 < / sub > < / sub > = 59.2%) (Pettijohn, 1972) I) andesite dacite distribution area II) the distribution area of Archean greywacke and slate. The sample number is the same as that in table 2-6

Fig. 2-16 (garnet, pyroxene) biotite plagioclase granulite (parametamorphic sample) 1g (W < sub > Na < sub > 2 < / sub > o < / sub > / W < sub > k < sub > 2 < / sub > o < / sub >) - 1g (W < sub > SiO < sub > 2 < / sub > / W < sub > al < sub > 2 < / sub > o < sub > 3 < / sub >) (simplified according to petizhuang et al., 1972)

a-greywackstone; B-lithic sandstone; C-sub arkose; D sub arkose sandstone; E-quartz sandstone 1) The samples of dacaoshachang migmatized supracrustal series have the same serial numbers as those in table 2-6 2) The samples in sihetang migmatized supracrustal series have the same serial numbers as those in table 2-9

Fig. 2-17 REE distribution patterns of garnet sub diopside biotite plagioclase granulite (97377) and Archean fi dacite (Fig. 2-18), W < sub > k < sub > 2 < / sub > o < / sub > / W < sub > Na < sub > 2 < / sub > o < / sub > - W < sub > SiO < sub > 2 < / sub > < / sub > diagram

OIA oceanic island arc; ACM - active continental margin; PM - passive continental margin. The sample serial number is the same as table 2-6

early Precambrian crystalline basement in Beijing area

a-oceanic island arc greywacke; B - continental island arc complex area; C - active continental margin greywacke area; D-the serial number of the samples in the greywacke area of the passive continental margin is the same as that in table 2-6

5.

1. The helostan group (PT < sub > 1 < / sub > h.)

is sporadically exposed in the southern part of Yecheng County, such as otulagyer and kalawashker, and is a regional metamorphic rock of amphibolite facies. The rock assemblages are mainly banded, eyeball shaped, striped and vein shaped gneiss, including biotite monzonite gneiss, biotite plagioclase gneiss, hornblende monzonite (plagioclase) gneiss, biotite monzonite shoshonite, etc. some sections are migmatized to varying degrees, intercalated with intermediate acid volcanic rocks. As a result of the multi-stage metamorphism and deformation, the overall layer is disordered, and the superimposed thickness is more than 1155 M

The

area is unconformably covered by the bochattage formation of Jixian system, which provides an important basis for determining the stratigraphic age. In addition, the isotopic age of the intrusive akazi pluton is 2261 + 95 / - 76 MA (Xu ronghua, 2000, zircon U-Pb upper intersection age), 2426 ± 46 MA (Zhang Chuanlin, 2003, zircon SHRIMP). The research level of this set of strata is relatively low, and it belongs to Paleoproterozoic at present

The elinkat group (PT < sub > 1 < / sub > a.)

is exposed in the middle reaches of tiekelamulong River, Bosten River and KELIYANG River, extending eastward to the south of Hotan. The rock assemblage is biotite quartz schist, dolomite quartz schist with garnet plagioclase quartz schist, and a small amount of shoshonite and marble. To the north of KANGXIWA, there are garnet biotite plagioclase gneiss, biotite monzonite gneiss and high amphibolite facies metamorphism. It contacts with the surrounding faults and is partially covered by the unconformity of the great wall system serragaztag group or the upper Devonian qizilaf formation, with a superimposed thickness of more than 1273 M. According to the field observation and comprehensive analysis, the original rock is argillaceous greywacke, which was formed in the littoral shallow sea environment, equivalent to the deposition of subtidal shallow sea shelf facies belt

There is no direct basis for the time. The spilite keratoporphyry intercalated with clastic rocks of the great wall system serragaztag group is unconformity with the group in bostengta River and sula'azigou. The isotopic age of the overlying potash keratoporphyry was 1764 MA (Wang Yuzhen, 1983), which is the Changcheng period. Therefore, the age of the underlying elinkat group was placed in the Paleoproterozoic

There is no direct contact between the helostan group and the elinkat group in the region. Both of them have undergone regional dynamic heat flow metamorphism of high greenschist facies and low amphibolite facies, with widespread migmatization, forming various crystalline schists, gneisses, and shoshonite. And the metamorphic degree of the former is deeper, whether the lower part of the former includes part of the Neoarchean still needs further work

The kulangna ancient rock group (PT < sub > 1 < / sub > K.)

is exposed in the West Kunlun Mountains, mainly distributed between the Kegang fault and the datongxi rock body, and is a medium and deep regional metamorphic rock with high greenschist facies and low amphibolite facies. The lower part is dominated by crystalline schist and quartzite with laminated magnetite quartzite, followed by marble and gneiss with a small amount of metamorphic volcanic rocks; The upper part is marble and andalusite schist. It contacts with the surrounding faults or is engulfed by the rock mass, and the superimposed thickness is more than 4871.6 M

This group is well exposed in the West Kunlun area, especially in Datong, kulangnagu River Basin and the north side of saitula. Marble graally increases from north to south in the region, and the superimposed thickness varies from place to place, and the thinnest part is 2990 M

the protolith is clastic carbonate rock intercalated with basic volcanic rock formation, which is littoral and shallow marine facies with weak volcanic eruption deposition

The U-Pb ages of zircons and K-Ar ages of the intrusive rocks are 480-495 Ma and 527.6 MA (1 ∶ 250000 Yecheng sheet), respectively. The characteristics of rock association and metamorphic degree are similar to those of the Tanan herostein group and the Karakoram brunkule group, so it is suitable to be placed in the Paleoproterozoic

The brunkule group (PT < sub > 1 < / sub > B.)

is the only Paleoproterozoic strata exposed in the Bayankala Qiangtang formation, which is distributed on both sides of the Yeerqiang River and in the north of yilik, and is a regional metamorphic rock of amphibolite facies. The lower part of the rock assemblage is light gray biotite quartz schist, biotite schist and eclogite bearing biotite quartz schist; The middle part is composed of garnet biotite quartz schist, cross garnet dolomite quartz schist, biotite quartz schist, sillimanite garnet biotite plagioclase gneiss, biotite plagioclase granulite with amphibolite; The upper part is biotite plagioclase granulite, hornblende biotite plagioclase granulite, plagioclase biotite quartz schist with marble. It is a set of parametamorphic rocks (khondalite series), and the protoliths are mainly clastic rocks. It is in fault contact with the surrounding strata, and the superimposed thickness is more than 13239 M. In the north of yilik, only the middle part of the group is exposed

According to the comparison of petrochemistry with Neoarchean and Paleoproterozoic, this group is close to Paleoproterozoic. U-Pb and Rb SR isochrons were used to determine the age of 2130-2700 MA in the metamorphic rocks of the equivalent group in Pamir, Southwest China

At present, there is another view about the formation age of the brenkule group. According to the heterogeneity of metamorphism, the great difference of rock association in different sections, and the early Paleozoic age information of detrital zircons collected from the strata (Zhou Hui, unpublished), it is considered that the early Paleozoic strata may be included in the group

The above-mentioned Archean Paleoproterozoic metamorphic stratigraphic fragments only represent the basic characteristics of the composition of the ancient basement materials in Tanan, Qin Qi Kun and Bayankala Qiangtang strata in the study area. There is little research on the internal relationship between them, and there is no unified or mature understanding at present

6.

The Anshan Group here refers to the Neoarchean supracrustal rock series distributed in the Anshan Benxi area, which is commonly referred to as "upper Anshan Group" or "middle and upper Anshan groups" by predecessors. The supracrustal rocks of Anshan Group are scattered in the granitic rocks of the same age but formed later in different scales, accounting for about 25%. The supracrustal rock series is characterized by a large number of banded quartz magnetite lean ores (Anshan type iron ores), so it is also called iron bearing rock series. There are large-scale rich iron ores in Gongchangling Mining Area. According to the rock association, Anshan Group is divided into Cigou formation, Dayugou formation and yingtaoyuan formation from bottom to top

The rock association, metamorphism, deformation and ore bearing characteristics of the

supracrustal series have some spatial changes (see Fig. 4-7). Cigou formation and Dayugou formation are distributed in Gongchangling, Benxi and Waitoushan in the East and northeast of the area. The total thickness of the strata is more than 2000m. The rock assemblages are mainly plagioclase amphibolite, biotite granulite and banded quartz magnetite lean ore, intercalated with garnet mica schist and quartzite, and a small amount of marble exists in Waitoushan and Gongchangling areas. Their protoliths are mainly volcanic sedimentary rocks such as basaltic and dacitic, with relatively few terrigenous sediments. There are many layers of quartz magnetite poor iron ore, but the thickness of single layer is small. The metamorphic grade is generally amphibolite facies or epidote amphibolite facies, and the deformation is also strong. Yingtaoyuan formation is distributed in East, West Anshan, Qianyan mountain and yingtaoyuan around Anshan area in southwest of the area, namely East-West Anshan ore belt and Qidashan ore belt. The rock thickness varies greatly in different positions, and the maximum is more than 800m. The rock assemblage is mainly mica quartz schist, phyllite and banded quartz magnetite lean ore, intercalated with amphibolite, quartzite and chlorite quartzite. Its protoliths are mainly high maturity muddy terrigenous clastic sedimentary rocks and a small amount of basaltic volcanic sedimentary rocks. The number of layers of iron ore is small, but the thickness of single layer is large. Generally, the metamorphic grade is epidote amphibolite facies and locally greenschist facies. The deformation is also relatively weak. According to the existing research, these different formations, which were once considered as the relationship between the upper and lower strata, may be the sedimentary procts of different places at the same time

The supracrustal series of Anshan Group was formed in the period of 2.65-2.75 GA. The main evidences are as follows: 1) for the whole rock SM nd isochron age determination of amphibolite in the supracrustal series of Anshan area and Waitoushan Beitai area, Qiao Guangsheng et al. (1990) obtained age data of 2.72 GA and 2.73 GA. In Gongchangling area, Liu Dunyi and song Biao et al. (1993) measured the detrital zircon of biotite granulite in the middle marker layer of supracrustal series by different methods, and obtained relatively concentrated age data of 2.50-2.70 GA. Although the biotite granulite was formed by sedimentary metamorphism, its protolith came from the contemporaneous intermediate acid volcanic rocks, so 2.70ga can roughly represent the formation age of the rocks, and some of the lower ages are related to the later metamorphism. 2) There are a lot of old granitic rocks in AnBen area. In Anshan, the supracrustal rocks are unconformity over the 2.97 GA Donganshan granite (Wu Jiashan et al., 1993). In Gongchangling, the supracrustal rocks are probably unconformity over the 2.99 GA Gongchangling gneissic granite (WAN Yusheng, 1993). They give the minimum age for the formation of the supracrustal series. 3) In Gongchangling area, many sets of detrital zircon ages greater than 3.00ga have been determined for epicrustal rocks, quartzites and chromite quartzites, which not only limit the age limit of rock formation, but also provide direct evidence for the origin of these detrital sedimentary rocks from ancient continental crust basement. 4) The supracrustal series is obviously intruded by 2.50ga potash granite (Liu Dunyi et al.), which indicates that the supracrustal series should have been formed before 2.50ga

in AnBen area, the rock association of the supracrustal rock series in Gongchangling iron ore area is the most representative, with more volcanic materials and terrigenous clastic sediments. It is for this reason, coupled with the existence of rich iron ore, many people have carried out in-depth and extensive research on the Gongchangling supracrustal rock series, and obtained a lot of practical data and new understanding (Cheng Yuqi et al., 1951, 1966, Zheng Baoding, 1956, Xu Guangrong et al., 1979, Li Shuguang et al., 1979, 1989, Shen Baoding et al ± Qing et al., 1981, Chen Guangyuan et al., 1983, Chen Xinrong, 1990, Wan Yusheng, 1993). This is highlighted below

the supracrustal rocks in Gongchangling iron ore area belong to the Cigou formation of Anshan Group, with an exposed area of about 7km < sup > 2 < / sup >. The deposit is divided into two parts: the second mining area and the Lingdong mining area. Among them, the study of the second mining area is more in-depth. From the bottom to the top, the second mining area is divided into the lower shallow grained rock section, hornblende rock section, the lower iron bearing rock section (composed of two iron ore layers and schist), the middle marker layer biotite granulite section (with the third iron ore layer), the upper iron bearing rock section (composed of three iron ore layers and two amphibolite layers), the siliceous rock section (with the seventh iron ore layer), and the upper shallow grained rock section. The protolith of the lower shoshonite member was once considered to be feldspar quartz sandstone, and the zircon age is 3.25-3.36 GA. regardless of age data or chemical composition, Cheng is very similar to the chentaigou granite in Anshan area. Therefore, it can not be ruled out that they are orthogneiss, which needs further study. According to the rock association, the supracrustal rock series in the second mining area can be divided into two volcanic sedimentary cycles. The boundary between the middle marker bed and the upper iron bearing rock section is taken as the boundary. Compared with the lower cycle, the terrigenous clastic sediments in the upper second cycle are more. Both of them constitute a large volcanic sedimentary cycle. In the Lingdong mining area, there are roughly the same stratigraphic sequence, but the upper part of the shallow grained rock and siliceous rock has been missing, and the middle marker layer is mainly garnet mica schist, rather than biotite granulite. According to the deep drilling and other data, the biotite granulite in the second mining area and the garnet mica schist in the Lingdong mining area are in the same layer transitional relationship

Plagioclase amphibolite is the main type of rock in Gongchangling supracrustal rock series. According to the characteristics of petrology and geochemistry, two types of amphibolites can be distinguished. They are distributed in the upper iron bearing section and the lower amphibolite section respectively. The composition of amphibolite in the upper part is uniform, usually massive and thick bedded, without micro bedding or compositional layer. The mineral assemblage is simple, mainly composed of amphibole and plagioclase. Some samples contain a small amount of quartz. The rock has a stable three-point meta crystalline structure. Its protolith is lava or basic tuff without obvious addition of terrigenous clastic material. In addition to amphibole and plagioclase, the lower amphibolite also contains more quartz and minerals such as biotite and garnet. Due to the layered distribution of different minerals, the rocks can show layered and banded structures. In the lower plagioclase amphibolite, there are hornblende granulite, biotite granulite and thin marble. The protolith is undoubtedly metamorphic basic tuff with terrigenous clastic materials

The chemical compositions of the two types of amphibolites are also quite different. The major element composition of the upper plagioclase amphibolite is similar to tholeiite, and it is located in the tholeiite area on the AFM map (Fig. 3-4A). There is a light rare earth depletion or flat rare earth pattern with low total rare earth content and no obvious Eu anomaly (Fig. 3-4b). The contents of incompatible elements Zr, Ti, Nb and P are not high, and the MORB normalized value is less than or close to 1 (Fig. 3-4d). In particular, there is a good linear relationship between LREE, HFS and other inactive incompatible elements (WAN Yusheng, 1993). On the Pearce diagram, large ion lithophile elements show obvious relative enrichment (Fig. 3-4d). According to the research of Zhai Mingguo et al. (1990), this type of basaltic rocks are also common in the entire AnBen area, and there are also rock samples (85 / A56, FIG. 3-4C and E) with obvious depletion of large ion lithophile elements, which can be almost completely compared with the depleted basalts of mid ocean ridge

Fig. 3-7 geochemical diagram of biotite granulite in Gongchangling area, Anshan City (quoted from Wan Yusheng, 1993)

a-ree model; According to the statistical results of 29 garnet mica schist analysis, the average chemical composition is: SiO < sub > 2 < / sub >: 63.29 (2.64), Al < sub > 2 < / sub > 2 < / sub > o < sub > o < sub > 3 < / sub > 3 < / sub >: 18.05 (P >

< p

P > P > 29 statistical results of garnet mica schist analysis, the average chemical composition is as follows: SiO < sub > 2 < / sub > 2 < / sub >: 63.29 (sub >: 63.29 (2.29 (2.64), Al < sub > 2 < / sub > 2 < / sub > 2 < / sub > o < sub > o < sub > o < sub > o < sub > o < sub > 3 < sub > 3 < sub > 3 < / sub > < p < p < p < p < p < p < p < p < p < p < p < p < p < p < p < p < p < p < p < p < p < p

(1), TiO < sub > 2 < / sub >: 0.66 (0.17) (in%, variance in brackets). Although the SiO < sub > 2 < / sub > constants of the rocks are very similar to those of biotite granulites derived from volcanoes, they are obviously different from the latter in terms of high Al < sub > 2 < / sub > o < sub > 3 < / sub >, K < sub > 2 < / sub > O > Na < sub > 2 < / sub > O. on a series of protolith discrimination diagrams, the rocks are put into muddy sedimentary rock areas (Fig. 3-6a and b). There is a strong negative Eu anomaly (Fig. 3-8a). In addition to Nb, Ba and P also show obvious relative depletion. BA is depleted relative to RB and th (Fig. 3-8b). In isotopic composition, the graphite of the four samples δ The 13C is - 2.6 ‰, which is of organic origin (Li Shuguang et al., 1983). There is no doubt that garnet mica schist has the characteristics of muddy and sandy rocks, and its protolith comes from the basement of continental crust with high maturity. Gneiss (lb9202-1) from Waitoushan Iron ore area is very similar to garnet mica schist from Gongchangling area (Fig. 3-8). The difference of their appearance reflects the different degree of metamorphism

Fig. 3-8 geochemical diagram of garnet mica schist in Gongchangling area, Anshan Benxi county, Yunnan Province, China; B-pearce diagram; Sample lb9202-1 was collected from Waitoushan area (data are shown in table 4-2a, B, c)

as mentioned above, biotite granulite and garnet mica schist in Gongchangling area are transitional in the same layer. Although the chemical compositions of the two types of rocks are quite different, there is an obvious transition phenomenon between them e to the combined action of material mixing and mechanical differentiation ring deposition. In Figure 3-6, the black triangle is the average chemical composition of 85 biotite granulites in AnBen area, which is located in the transitional zone of two types of clastic sedimentary rocks, indicating that the mixing of different source materials and the differentiation of mechanical deposition also exist in the region

Quartz magnetite poor ore usually has a clear striped or banded structure, which is mainly composed of magnetite and quartz. Mafic amphibole is a common mineral, and there are also actinolite, chlorite and garnet. The chemical composition is characterized by rich silicon and iron. The normalized values of chondrites are less than 10, usually between 2 and 5, and there are obvious positive EU anomalies. Many research results show that the protolith of quartz magnetite poor ore is of chemical sedimentary origin, and the source of ore-forming materials is closely related to iron rich basaltic volcanism, which is the result of volcanic exhalation and volcanic hydrothermal action accompanied by volcanic activity

7.

It is widely distributed in Jiaobei stratigraphic District, and it is distributed around Archean metamorphic rock series, with stable lithology and good continuity. There are three lithostratigraphic sequences: Jingshan group, fenzishan group and Zhifu group. Although the relationship between groups is not clear, the relationship among groups is clear. The Jingshan group is unconformity ctile shear overlying the Neoarchean Qixia superunit; The fenzishan group, Qixia superunit and Jingshan group are all in ctile shear structural contact. The Zhifu group is less exposed and limited. It is separated from the fanzishan group by quaternary system and cut through by Paleoproterozoic and Neoproterozoic intrusive rocks. The first two groups are the occurrence horizons of graphite, magnesite, talc and marble in Shandong Province. The relationship between the fanzishan group and the Jingshan group is controversial, but most of them are considered to be the procts of different facies at the same time, and the three belong to the normal clastic carbonate deposits of Paleoproterozoic rift trough

The Paleoproterozoic Jingshan group (PT < sub > 1 < / sub > J)

the Jingshan group is a nearly EW island or fault block distributed in the southern margin of Jiaobei stratigraphic District, such as Jingshan and jingqishan in Laiyang, Mingcun and Xianshan in Ping, Nanshu in Laixi, Guangshan and Xiangshan in Muping, Jingshan in Haiyang, tading in Qixia, Wuji in Rushan, etc; It is unconformity ctile shear, overlying the tTG granite series of the Neoarchean Qixia super unit, and in contact with the fenzishan group as a ctile shear structure; It was cut by Paleoproterozoic and Neoproterozoic intrusive rocks and covered by unconformity of Laiyang group in Early Cretaceous; It consists of a suite of high alumina schist, granulite, diopside, marble and graphite bearing rock series. The regional extension is stable and the fold deformation is strong, which often constitutes superimposed fold structure. From bottom to top, they are divided into lugezhuang group (PT < sub > 1 < / sub > JL), yetou group (PT < sub > 1 < / sub > JY) and Douya group (PT < sub > 1 < / sub > JD). Each group is divided into two segments, and the relationship between groups and segments is integration (table 2-1). The total thickness is 3339m

(1) the lugezhuang formation (PT < sub > 1 < / sub > JL) is unconformity ctile shear overlying the Neoarchean Qixia superunit, and is in conformity with the overlying yetou formation. The lower Anji village schist member (PT < sub > 1 < / sub > JL < sup > a < / sup >): Garnet sillimanite biotite schist intercalated with biotite schist, garnet biotite granulite, graphite bearing garnet sillimanite biotite schist, diopside granulite and marble, with a thickness of 1272m; The upper Guangshan marble member (PT < sub > 1 < / sub > JL < sup > G < / sup >): serpentinized marble, dolomitic marble intercalated with diopside marble, olivine marble and diopside marble, 447M thick. There are differences in the exposure of the group in different places, and the upper or lower segment is missing. The total thickness is 1719m

(2) the yetou formation (PT < sub > 1 < / sub > JY) is integrated with the underlying lugezhuang formation and the overlying Douya formation. The lower Xiangshan granulite member (PT < sub > 1 < / sub > JY < sup > x < / sup >): Diopside biotite granulite, epidotized biotite granulite, diopside intercalated with feldspar quartzite, diopside diorite, shoshonite and marble lens, 634m thick; The upper dingguosi marble member (PT < sub > 1 < / sub > JY < sup > d < / sup >): dolomite marble, serpentinized marble, diopside marble with diopside, calcite marble, 540M thick. The main lithology of each section is stable, only the interlayer varies from place to place, with a total thickness of 1174m

(3) Douya formation (PT < sub > 1 < / sub > JD): except for Jingshan and mupingxiangshan in Laiyang, there are only graphite Series in other places. There is no relationship with overlying strata. The lower Xucun graphite rock series (PT < sub > 1 < / sub > JD < sup > x < / sup >): Graphite biotite granulite, graphite biotite plagioclase gneiss, graphite diopside granulite intercalated with feldspar quartzite and marble, 329m thick; The upper shuitaolin schist member (PT < sub > 1 < / sub > JD < sup > s < / sup >): sillimanite garnet biotite schist, garnet biotite schist, bluecrystal garnet biotite plagioclase gneiss, 117m thick. The number of graphite bearing layers varies in different parts of the section, which is the occurrence layer of Jiaodong crystalline graphite ore, with a total thickness of 446m

The Jingshan group is surrounded by the Neoarchean Qixia superunit, which is a part of the ancient crystalline basement and the occurrence horizon of graphite ore in the province. In addition, talc, diopside and marble ornaments are also considerable. The obvious dichotomy of the three components indicates that the group is composed of three transgressive cycles. The protolith series is a set of high alumina, carbon rich clay, sand and other clastic deposits carbonate deposits, belonging to flysch like carbonate formation, with high degree of metamorphism of amphibolite facies and local amphibole granulite facies. It is a set of khondalite series that has undergone high-grade metamorphism. Most of them are open longitudinal bend folds composed of similar syncline and inversion folds with obvious superimposition and developed bedding ctile shear structures. The isotopic ages are mainly between 1847 and 2478 Ma, so they belong to Paleoproterozoic

The Paleoproterozoic fanzishan group (PT < sub > 1 < / sub > F)

is another Paleoproterozoic group lithostratigraphic unit similar to Jingshan group in lithologic association in Ludong stratigraphic division. It is distributed in Laizhou fanzishan, Penglai jinguoshan, southern Yantai, Fushan and qixiamiaohou along the northern coast of Jiaobei stratigraphic District, and sporadically distributed in Ping Huibu, It is composed of an ancient metamorphic basement and a set of bedded metamorphic rock series with nearly East-West distribution. It is mainly composed of iron bearing rock series, granulite, schist, shoshonite, feldspar quartzite, diorite, marble, graphite bearing rock series intercalated with magnesite and talc. It is in contact with the underlying Neoarchean Qixia superunit and Jingshan group in ctile shear structure, and has no clear relationship with Zhifu group. It is cut by Paleoproterozoic and Neoproterozoic intrusive rocks and is divided into Xiaosong formation (PT < sub > 1 < / sub > F X) from bottom to top In zhujiakuang group, < inlinemediaobject > < imageobject > < imagedata role = "3" fileref =. / image / figure-0033-0001. JPG "> < title > < / Title >

< / picdesc > < / imagedata > < / imageobject > < / inlinemediaobject >, < image / figure-0033-0001 There are five lithostratigraphic units in Zhanggezhuang formation, which are < inlinemediaobject > < imageobject > < imagedata role = 3 "fileref =. / image / figure-0033-0002. JPG > < title > < / Title >

< / picdesc > < / imagedata > < / imageobject > < / inlinemediaobject >, jutun formation (PT < sub > 1 < / sub > F J) and Gangyu formation (PT < sub > 1 < / sub > F G), There are great differences in the development and thickness of each group in different areas. The total thickness is 2000-3393m

(1) Xiaosong formation (PT < sub > 1 < / sub > FX): the NE trending narrow belts are intermittently distributed and contact with the underlying Qixia superunit as fault or ctile shear structure. The lithology is biotite granulite, biotite hornblende granulite, plagioclase amphibolite intercalated with electric sillimanite, feldspar quartzite, magnetite quartzite, sillimanite schist, occasionally intercalated with diorite marble and metamorphic conglomerate. The lithology and thickness vary greatly in the area, and the formation is the iron ore horizon in Jiaobei area

(2) zhujiakuang formation < inlinemediaobject > < imageobject > < imagedata role = "3" fileref =. / image / figure-0033-0003. JPG > < title > < / Title >

< / picdesc > < / imagedata > < / imageobject > < / inlinemediaobject >: Miaohou and jingguoshan areas have ctile shear structural contact with underlying Qixia superunit, and Dazhuangtou area has ctile shear structural contact with Jingshan group lugezhuang formation. The lithology is composed of shoshonite, feldspar quartzite, biotite granulite with garnet sillimanite biotite schist, diorite, marble and graphite bearing biotite plagioclase gneiss

(3) Zhanggezhuang formation < inlinemediaobject > < imageobject > < imagedata role = "3" fileref =. / image / figure-0034-0001. JPG > < title > < / Title >

< / picdesc > < / imagedata > < / imageobject > < / inlinemediaobject >: the rock association can be divided into three sections from top to bottom. The first member is dolomite marble, diorite marble with feldspar quartzite and biotite granulite; The second member: diorite schist, biotite granulite, diorite granulite with biotite schist and talc diorite; The third member is dolomite marble intercalated with biotite schist and sericite quartz schist. The fanzishan area is dolomite marble, magnesite, talc schist and talc chlorite schist. The lithology of the formation is stable and rich in magnesium. It is the occurrence horizon of magnesite and talc

(4) jutun formation (PT < sub > 1 < / sub > FJ): it is characterized by fine crystalline graphite, and its lithology is graphite biotite granulite, graphite calcite marble, graphite diorite, graphite diorite granulite, graphite biotite schist with biotite granulite, diopside quartzite, etc

(5) Gangyu formation (PT < sub > 1 < / sub > FG): it is covered by unconformity of Sinian Penglai group, and its lithology is pimple like garnet silica line biotite schist, biotite schist, biotite schist intercalated with biotite granulite, feldspar quartzite, etc

The fanzishan group is characterized by nearly EW trending open compound longitudinal bend folds, developed bedding ctile shear structures, similar rock assemblage to Jingshan group, and its protoliths are aluminum bearing sand, argillaceous clastic rock, magnesium rich carbonate rock, calcium magnesium silicate, carbonaceous and argillaceous clastic rock, belonging to flysch like carbonate sedimentary formation, A set of intermediate metamorphic khondalite series is formed by regional amphibolite facies metamorphism. The isotopic ages range from 1848 Ma to 2478 Ma, belonging to Paleoproterozoic. It is the occurrence horizon of magnesite, talc and metamorphic sedimentary iron ore in Shandong Province

3. Zhifu group < inlinemediaobject > < imageobject > < imagedata role = "3" fileref =. / image / figure-0034-0002. JPG > < title > < / Title >

< / picdesc > < / imagedata > < / imageobject > < / inlinemediaobject >

has less exposure, and is limited to Yantai Zhifu Island, Kongtong island and nearby small islands. It is a suite of quartzite bearing Specularite rock assemblage, which can be divided into three groups, The lower LAOYESHAN formation is composed of potash feldspar quartzite, Specularite quartzite, dolomite quartz schist, dolomite potash feldspar gneiss, gravelly potash feldspar quartzite, dolomite schist and marble; The central Bingying formation is composed of thick bedded quartzite, K-feldspar quartzite intercalated with tourmaline bearing quartzite, top dolomite quartz schist, biotite granulite and marble; Upper Dongkou formation < inlinemediaobject > < imageobject > < imagedata role = "3" fileref =. / image / figure-0034-0005. JPG > < title > < / Title >

< / picdesc > < / imagedata > < / imageobject > < / inlinemediaobject >: thick bedded potash feldspar quartzite and quartzite. The original rock series is a set of well sorted terrigenous clastic rocks, belonging to terrigenous clastic intercalated carbonate sedimentary formation. The metamorphism reached low amphibolite facies. The isotopic age is 2171 ma. It belongs to Paleoproterozoic, with a total thickness of 1632m

8. In metamorphic rocks, there are some inclusions of fine minerals in a larger mineral crystal (usually phenocryst). These inclusions are usually formed earlier than or at the same time with the phenocryst. Large minerals are often called main crystals, and small minerals are called guest crystals. This kind of structure is called poikiloblastic texture. There are several equilibrium symbiotic relationships among main crystal minerals, guest crystal minerals (mineral inclusions) and other minerals in metamorphic rocks, which are described as follows< The minerals in the inclusions not only exist in the main crystal minerals, but also distribute in the rocks, which are in direct contact with other minerals in the rocks. The minerals in the inclusions and the minerals in the rocks form a mineral paragenetic Association. The main minerals of biotite epidote albite schist in Shandong Province (photo 9-24) are albite, epidote, chlorite, biotite and a small amount of actinolite. The inclusion minerals in albite phenocrysts are columnar epidote and actinolite, which are oriented in the phenocrysts, and their direction is consistent with the schistosity of the rock, The mineral assemblage of the rock is: albite + actinolite + epidote + chlorite + biotite, that is, the optical characteristics and directional distribution of epidote, actinolite and other inclusions in albite phenocrysts are uniform with epidote, actinolite and other minerals in the rock matrix, and the inclusion minerals epidote and actinolite are consistent with other minerals in the rock, In order to balance the symbiotic relationship< The inclusion minerals only exist in the main crystal minerals and do not contact with other minerals in the rocks. The main crystal mineral is a shield to prevent the inclusion minerals from contacting with other minerals in the rock. The main crystal mineral and the inclusion minerals are in local equilibrium mineral paragenesis, while the inclusion minerals and other minerals in the rock do not belong to the same mineral paragenesis Association. In the garnet biotite K-feldspar gneiss in Antarctica, fine needle like sillimanite is directionally distributed in the phenocrysts of garnet, and does not contact with other minerals in gneiss, forming two locally balanced mineral paragenetic assemblages of garnet + sillimanite and garnet + biotite + K-feldspar + quartz (photo 9-26)
the garnet phenocryst inclusions in garnet biotite monzonite gneiss in TAIPINGZHAI area, Hebei Province include sillimanite, corunm and dark green spinel (photo 9-28). Among them, the fine acicular sillimanite inclusions are distributed directionally, and their direction is basically parallel to the gneiss of the rock. The minerals in gneiss are garnet, biotite, plagioclase, plagioclase and quartz. There are no corunm, spinel and sillimanite minerals in gneiss (photo 9-27). It can be seen that the mineral associations in the rocks are garnet + biotite + plagioclase + plagioclase + quartz and garnet + corunm + spinel + sillimanite. Sillimanite, corunm and spinel are associated with garnet in local equilibrium (photo 9-28), but sillimanite, corunm and spinel do not belong to the same mineral association with other minerals in gneiss
the paragenetic relationship between the minerals of different occurrence indicates that there was sillimanite in the rocks before the formation of gneiss. Due to the depletion of sillimanite when it was transformed into other minerals in the metamorphic reaction, part of the sillimanite wrapped in garnet could not continue to participate in the metamorphic reaction and was preserved. Corunm and spinel are SiO2 poor minerals. Because there is quartz in gneiss, corunm, spinel and quartz are incompatible minerals, so they cannot coexist in equilibrium. Thus, corunm and spinel can only exist as inclusions in garnet phenocrysts in gneiss containing quartz.

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