The Tuwu-Yandong porphyry copper deposit in Xinjiang is regarded as an important breakthrough in prospecting in Xinjiang, and a lot of work has been invested and many research results have been published. However, there are still many disputes about the metallogenic age and its relationship with tectonic activities, especially the metallogenic age. Rui Zongyao et al. (2002) obtained Rb-Sr isochron of ore-bearing porphyry (plagioclase granite porphyry) and U-Pb isotopic age of single zircon, which belongs to Late Devonian. The Sm-Nd isochron and single zircon U-Pb isotopic age of ore-bearing volcanic rocks are between 4 16 ~ 360Ma, belonging to Devonian. The Re-Os isochron age of chalcocite in ore is (322.7±2.3)Ma, which belongs to the product of Early Carboniferous. The zircon U-Pb ages of Chihu plagioclase granite porphyry are (292.13.5) Ma and 283.5Ma (Ren Bingchen et al., 2002), and the Rb-Sr ages of Penguinshan granodiorite are (287±42)Ma and (1.995). Qin et al. (2002) obtained that the altered mineralized plagioclase granite porphyry of Tuwu-Yandong porphyry copper mine has a zircon U-Pb age of (356 8) Ma, an altered sericite K-Ar age of (34 1.2 1.4)Ma and an ore-bearing age of (39Ar/40Ar). The U-Pb isotopic harmonic curve of a single zircon measured in the plagioclase granite porphyry in the east of Tuwu copper mine (TC42 trough) is (30 1 13) Ma, and the emplacement age of the rock mass is late Carboniferous (Li Wenming et al., 2002). Chen Yuchuan et al. (2003) thought that the existing age data changed greatly, whether it reflected the complexity of the test problem or the structural evolution itself needs further discussion, but volcanic rocks contain zircon information of multiple ages, which makes it difficult to determine the diagenetic age. There are three groups of relatively concentrated ages: 434 ~ 426 Ma, 334.6~320Ma and 260Ma, in which the early and late groups may reflect two magmatic events, while the middle group may represent the age of volcanic formation.
In a word, there are different views on metallogenic strata and metallogenic age, all of which belong to Hercynian period, and there is no evidence of Indosinian or Yanshanian mineralization. Based on the fission track analysis of zircon and apatite, the work of this book will discuss the metallogenic age, metallogenic stages and tectonic activities in this area, and gain a new understanding that there are many mineralization in this area, and the Indosinian and Yanshanian mineralization is still possible.
Second, the geological characteristics
The East Tianshan Mountains, located in the southern margin of the ancient Asian Ocean, is the gathering area of the Siberian plate and the Tarim plate. During the long-term evolution, it has experienced extremely complicated cracking and assembly, and has a variety of tectonic environments. The Tuwu-Yandong large-scale porphyry copper deposit in Xinjiang is located in the north of Kanggurtag deep fault and the south of Dacaotan fault, with the geographical coordinates of 9215 ′ ~ 93 05 ′ east longitude. The northern latitude is 42 00 ′ ~ 4215 ′, which belongs to the island arc belt of Da Nanhu accretion and collage in the late Paleozoic in the East Tianshan Mountains. This area is dominated by fault structures. Dacaotan fault zone and Kanggurtag fault zone are regional large faults passing through this area, and the overall trend is close to east-west, and the east is slightly north, showing NEE direction. To the north of Dacaotan fault are volcanic rocks of Dananhu Formation of Lower Devonian and sedimentary rocks of Tousuquan Formation of Middle Devonian. Carboniferous Gandun Formation sedimentary rocks are exposed in the south of Kanggur fault. Devonian Penguin Mountain Group is the main fault between the two main faults, and its lithology is basalt, andesite, andesite breccia lava, volcanic breccia, lithic sandstone, composite conglomerate and tuff. Devonian strata are directly covered by Jurassic carbonaceous rock series (Figure 1-4-26). From bottom to top, it can be divided into three lithologic sections: ① Basic lava with neutral lava section: from early eruption of volcanic breccia and tuff to thick basic lava with neutral lava. ② Volcanic detritus-sedimentary rock section: about 500m thick, consisting of basic tuff, tuff sandstone, sedimentary tuff, gravelly tuff sandstone and volcanic conglomerate. It is formed by pyroclastic and terrigenous clastic, and the lithofacies changes greatly. ③ Lithologic profile of interbedded basic lava and neutral lava with pyroclastic rocks: huge thickness, consisting of several eruptive periods (lava) and intermittent periods (pyroclastic rocks) (Ren Bingchen et al., 2002). The occurrence of strata is inclined to the south with an inclination angle of 43 ~ 63. Late Paleozoic intrusive rocks are widely distributed in this area. Another feature is that in the Kanggurtag deep fault and its vicinity, the foliation is particularly developed, and its occurrence is basically consistent with the stratum.
Ore bodies occur in pyroclastic sedimentary rocks, and the mineralized surrounding rocks include diorite, plagioclase granite porphyry and volcanic sedimentary rocks. Porphyries include plagioclase granite porphyry and diorite porphyry. The occurrence space of these rock bodies is mainly concentrated in volcanic-sedimentary rock sections, and the rock bodies are veinlets, rock plants and rock nodules. Most sections of plagioclase granite porphyry are covered by glutenite, which shows that plagioclase granite porphyry has transverse diorite porphyry. Among the host rocks, about 20% are porphyritic-porphyritic sodium acidic intermediate-acidic subvolcanic rocks (albite porphyry and quartz porphyry), and the copper grade of ore bodies is relatively high. Sodium intermediate-acidic intermediate-basic volcanic rocks and subvolcanic rocks (andesite porphyrite) with granular interwoven structure account for about 50%; Al-rich volcanic rocks (high-alumina basalts) account for about 20%, of which the copper grade of ore bodies is low; Sodium intermediate-acidic intermediate-basic pyroclastic rocks with tuff texture and clastic texture account for about 65,438+00% (Chen Wenming et al., 2002). The ore-hosting rocks are characterized by being rich in sodium, aluminum and potassium, with obvious albitization, silicification, chloritization, epidotization and carbonation. There are two ore bodies in the alteration zone: the surface control length of No.1 ore body is 1400 m, and the maximum width is 135.7 m. The depth and extension of the deep part are very large. The copper grade is 0.20% ~ 1.92%, with an average of 0.59%, accompanied by silver and gold. The surface control length of No.2 ore body is1300m, and the maximum width is 84.15m. The average grade of copper is 0.30%. The ore body is thick and inclined to the south, with an inclination angle of 65 ~ 8 1. Yandong Copper Mine is located at 10km to the west of Tuwu Copper Mine, which has the same characteristics as Tuwu Copper Mine. The average copper content on the surface is 0.32%, the cumulative ore thickness of ZK00 1 hole is about 557m, and the average copper grade is 0.5%, accompanied by aluminum, gold and silver. There is no natural boundary between ore bodies and surrounding rocks, but a gradual relationship, and the mineralization inside and outside the surface is constantly evolving.
Figure 1-4-26 Regional Geological Schematic Diagram of Tuwu-Yandong Porphyry Copper Deposit in East Tianshan Mountain
(Quoted from Zhang Lianchang et al., 2004)
Three. Samples and experimental results
Through the Tuwu-Yandong large porphyry copper mine area and the Kanggurtag fault zone and Dacaotan fault zone on its north and south sides, the fission track sampling analysis of apatite and zircon in the regional profile was carried out. The research profile is located at 92 36 ′ 30 ″ ~ 92 40 ′ 20 ″ east longitude and 42 03 ′ 21″ ~ 42 09 ′ 40 north latitude.
The collected rock samples are crushed, and the particle size after crushing should be suitable for the particle size of minerals in the rock, which is generally about 60 meshes. Single minerals are roughed by traditional methods and purified by electromagnetic separation and heavy liquid separation. Zircon and apatite have different experimental methods. Zirconite is hot-pressed by perfluoroethylene propylene. Put several zircon particles on the glass slide, heat and bake for 4 ~ 5 minutes, cover a piece of perfluoroethylene propylene plastic with a thickness of about 0.5mm, and then cover another glass slide to embed zircon particles in the plastic sheet. After cooling, the perfluoroethylene propylene plastic sheet was removed from the glass slide, and then ground and polished. Etching with KOH+NaOH solution at 2 10℃ for about 25 h, exposing spontaneous tracks, which can be observed by professional optical microscope. Radioneutron fluence is calibrated by the N2 international standard uranium glass method (Bellemans et al., 1994). For apatite, put apatite particles on a glass sheet, drop epoxy resin, and then grind and polish to expose the inner surface of the mineral. At 25℃, it was etched with 7% nitric acid for 30s, showing spontaneous tracks. The low-uranium muscovite external detector and mineral I were combined into the reactor for irradiation, and then the induced track was shown by etching with 40% HF for 20s at 25℃. Neutron fluence is calibrated with CN5 uranium glass. With the AUTOSCAN automatic measuring device imported from Australia, the density of spontaneous track and induced track is measured by selecting a cylinder parallel to the C axis, and the length of horizontal closed track is measured according to the procedure suggested by Green( 1986) (Gleadow et al., 1986). The age value is calculated according to the ξ constant method recommended by IUGS and the standard fission track age equation (Hurford and Green, 1982). The fission track of minerals is measured by high-precision optical microscope at high magnification, and the correct identification of fission track is very important.
Nine zircon fission track analysis results (table 1-4-7) and seven apatite fission track analysis results (table 1-4-8) were obtained. Except for the red granite porphyry (K78-3), the P(x2 test values of other samples are much greater than 5%, indicating that they belong to the same age group. The lithology of the samples includes conglomerate, schist, volcanic rock and granite porphyry. Except for the 1 apatite sample (K80) taken from the northern part of Dacaotan fault zone, the rest samples were taken from the Da 'nan Lake accretionary collage island arc zone between Dacaotan fault zone and Kanggurtag fault zone. Zircon fission track ages are 158 ~ 289 Ma, of which 7 samples are concentrated in 200 ~ 289 Ma, and the zircon ages of the samples are also younger than their stratigraphic ages, reflecting that they are the result of late thermal events. In the fault zone, the strongly foliated schist is also 222Ma, and the strongly foliated volcanic rock is 220Ma. The age of granite porphyry vein and tuff in Tuwu mining area is (276±26)Ma and (289±29)Ma respectively. Two younger samples were strongly altered, of which K78-3 was taken from the red granite porphyry in the exploration trench. Redness is the result of oxidation of metal minerals, and at the same time it has strong silicification, which should belong to mineralization alteration. Therefore, zircon age reflects two thermal events, namely, 200 ~ 289 Ma and 158 ~ 165 Ma.
Table 1-4-7 zircon fission track analysis results
Table 1-4-8 apatite fission track analysis results
The fission track age of apatite is 64 ~140ma, in which the strong schist in the fault zone is (97 9) Ma, and the altered andesite and dacite are (10410) Ma and (135/kloc-0) Ma respectively. The conglomerate on the north side of the mining area is (13214) ma; The apatite fission track age of andesite porphyrite K80 located on the north side of Dacaotan fault zone is the youngest, only (64 6) Ma.
Four. Metallogenic stage
Figure 1-4-27 not only reflects the relationship between zircon fission track age and altitude, but also shows the age distribution of each sample. It can be seen from figure 1-4-27 that zircon ages are divided into three age groups, namely, ① 289 ~ 276 Ma, ② 232 ~ 200 Ma, ③ 165 ~ 158 Ma. The altitude of the first and third age groups is small, with little change; The altitude of the second age group varies greatly. Similar to figure 1-4-27, the relationship between apatite fission track age and altitude (figure 1-4-28) also shows three age groups: 140 ~ 132 Ma, 109 ~ 97 Ma and 67 ma. On the one hand, it shows that the second age group represented by zircon and apatite ages is more important and active in this area; On the other hand, it shows that the three age groups reflected by zircon and apatite age actually have a corresponding relationship, that is, the age corresponding relationship when zircon sealing temperature drops from 250℃ to apatite sealing temperature 100℃ (table 1-4-9).
Table 1-4-9 Three Periods Reflected by Fracture Trajectory Analysis of Zircon and Apatite
Figure 1-4-27 Relationship between zircon fission track age and sample elevation
Figure 1-4-28 Relationship between apatite fission track age and sample elevation
Mineralized diorite porphyrite Fe2O3/(FeO+Fe2O3) = 0.52 ~ 0.53, and plagioclase granite porphyry Fe2O3/(Fe2O3+FeO) = 0.80 ~ 0.87, indicating that the formation and mineralization of the rock mass occurred on the shallow surface. The metallogenic temperature of the mining area is 120 ~ 350℃ (Wang Fu equals, 200 1). The closed temperature of zircon fission track is 250℃, and the temperature of annealing zone is generally between 200℃ and 350℃, so the age of zircon fission track can represent the metallogenic age. Therefore, we think that the three thermal events of 289 ~ 276 Ma, 232 ~ 200 Ma and 165 ~ 158 Ma in Tuwu copper mine area are probably metallogenic thermal events. Zircon and apatite correspond to each other in three age groups, and their longitudinal duration (that is, from 250℃ to 100℃) varies from 1, 2 to 3, which are about 146Ma, 108Ma and1000 ma, respectively, from early morning. Compared with Altai area, the vertical duration of Tuwu copper mine area is longer. The samples are mainly ores and mineralized altered rocks in the mining area, and the age of the samples in the adjacent area is consistent with that in the mining area, which should be the embodiment of metallogenic activities and tectonism in this area and consistent with that in Altai area.
According to zircon SHRIMP age, molybdenite Re-Os isochron age, altered sericite K-Ar age and timely Ar-Ar age, the latest research results in Tuwu copper mine area suggest that the diagenetic age of plagioclase granite porphyry is 36 1 ~ 333 Ma, the metallogenic age of porphyry copper mine is 347 ~ 323 Ma, and the main metallogenic age is 347 ~ 343 Ma (Zhang Lianchang et al. (spindle), wheat seed. (wheat) and so on. It is confirmed that the metallogenic age of Tuwu copper mine should not be earlier than the Late Carboniferous. Therefore, there is a contradiction between the above metallogenic age and fossil age. One of the reasons may be that the sealing temperature of SHRIMP age and Ar-Ar age is much higher than the metallogenic temperature. The metallogenic temperature of the mining area is 120 ~ 350℃, the age closing temperature of zircon fission track is 250℃, and the age group of 1 period is 289 ~ 276 Ma, which is consistent with the age of ore-bearing strata fossils.
Of course, the zircon fission track age mentioned above may be the result of annealing transformation caused by late tectonism, and does not represent mineralization. If so, at least the same mining area should have the same or similar age, but this is not the case. Zircon fission track ages of three ore-forming plagioclase granite porphyries in the mining area are (276±26)Ma, (23219) Ma, (16515) Ma, (289±29)Ma, and dacite is 200Ma. It can be seen that the same mining area has different ages, especially the mineralization age of plagioclase granite porphyry is obviously different, which should belong to different metallogenic periods. The younger samples of zircon in the third stage are plagioclase granite porphyry mineralization veins and mineralized altered dacite, which are strongly altered ore samples and the result of mineralization activities, so they directly represent the metallogenic age. For example, the sample K78-3 with the age of 165Ma is taken from the red mineralized granite porphyry in the exploration ditch, which is characterized by metal mineralization, surface silicification and linear silicification. It can be seen that the late mineralized vein penetrates and is also red, but it is linear carbonation without silicification. Obviously, K78-3 belongs to metallogenic samples.
The above three metallogenic stages in this area are consistent with the metallogenic age in Altai area. Because they are all in the same regional tectonic background, they have the same metallogenic period and age. In addition, the zircon U-Pb ages of Chihu plagioclase granite porphyry are (292.65438±0.3.5)Ma and 283.5Ma, respectively, and the single zircon UPb age of Penguinshan quartz diorite is 308.52Ma (Ren Bingchen et al., 2002). The gold mineralization age found in Kanggurtag ductile shear zone is 244 ~ 288 Ma (Qin et al., 2002), which also indicates the possibility of early Permian mineralization. At the same time, the existence of Indosinian and Yanshanian magmatic rocks in the area shows that it is reasonable to have mineralization corresponding to magmatic activities.
As mentioned above, the ages of zircon and apatite correspond to each other. The fission track closure temperature of apatite is 100℃, and the mineralization temperature of the mining area is 120 ~ 350℃ (Wang Fu equivalent, 200 1), so the fission track age of apatite may represent the thermal activity after mineralization. The apatite fission track ages of two mineralized plagioclase granite porphyries (samples K7 1-2 and K77) are 140Ma and 109Ma, respectively. The zircon fission track ages of these two samples are 276Ma and 232Ma, respectively, and the age difference between zircon and apatite (that is, the longitudinal duration of the two samples) is 65438±09ma, respectively.
Tuwu mining area has multi-stage mineralization and long duration, which can also be proved by the characteristics of the deposit. First of all, Tuwu copper mine has experienced multi-stage alteration, at least two stages of porphyry mineralization alteration (Yang Xingke et al., 2002), which is consistent with the different ages and characteristics of metallogenic porphyry bodies. In addition, the ore bodies occur in volcanic sedimentary rocks, subvolcanic diorite porphyry and plagioclase granite porphyry, indicating that submarine hot spring activity, subvolcanic hydrothermal solution and mineralization of plagioclase granite porphyry all provide ore-forming materials; In addition, Qin et al. (2002) pointed out that it is likely to be deep and late superimposed mineralization, that is, there is secondary mineralization in this area, which deserves attention. Combined with some similarities in metallogenic characteristics and ore-controlling factors of Getong gold deposit in northern Carata, they may form a porphyry-subvolcanic mountain-epithermal metallogenic belt. Therefore, multi-stage magmatic activity and mineralization superposition are not only the dominant factors of huge metal accumulation, but also the reasons for the existence and long duration of multi-stage mineralization.
Verb (abbreviation of verb) is the period of construction activity.
The latest research results of Chen Wen et al. (2005) show that the age of shear deformation is inferred from the strata involved in the ductile shear zone and the related Rb-Sr and K-Ar isotopic dating results. However, due to the limitations of the adopted geochronology method, the data obtained are large in scope and lack of accuracy. The 40Ar/39Ar dating technique, which is most suitable for structural deformation dating, proves that the Qiugemingtash-Huangshan ductile shear zone has multi-stage activities. The early compressional nappe shear occurred after 300Ma and ended at 280.2Ma In the late dextral strike-slip shear deformation, the auxiliary active period is 247.5438+0 ~ 242.8ma.. Considering that the 40Ar/39Ar age of mylonite is higher than that of zircon fission track, the two active stages of 300~280.2Ma and 247. 1 ~ 242.8ma should be consistent with the two metallogenic stages of zircon fission track method mentioned above, namely, 289~276Ma and 232~200Ma. Of course, zircon age also recorded another thermal event of 165 ~ 158 Ma.
Therefore, the mineralization stage in Tuwu area is consistent with the tectonic activity stage, and the fission track study shows that there are three stages in total. According to the characteristics of regional geological evolution (Xiao et al., 2003; Laurent-Charvet et al., 2003; Xu et al., 2003), 1 The tectonic-metallogenic period is related to the subduction-collision of the late Paleozoic plate in the eastern Tianshan Mountains, and the later period is controlled by post-collision intracontinental orogeny.
Fig. 1-4-29 Relationship between apatite fission track age and distance from fault zone samples.
If the distance between the north and south phases of the sample is plotted by apatite age and zircon age (Figure 1-4-29, Figure 1-4-30), the apatite age-distance diagram (Figure 1-4-29) shows that the fault zone in this area controls the sample. On the diagram of zircon age and distance (figure 1-4-30), with the change of distance, the age changes little, indicating that the fault zone has little influence on zircon age, probably because the closing temperature of zircon age is high and the consistent influence is not obvious. However, the ages of the samples in the south of the copper mine area are very close, with the ages of the three samples ranging from 200 to 200 to 222 Ma, while the ages of the samples in the mining area are quite different, ranging from158 to 289 Ma (Figure 1-4-30).
Figure 1-4-30 Relationship between zircon fission track age and sample distance
Figure 1-4-3 1 Thermal History of Geological Evolution in Tuwu Area
The abscissa is time/mA and the ordinate is temperature/℃. The figures in the figure represent the number of samples, measured length and simulated length, measured age and simulated age, K-S and GOF (Kolmogorov-smirnoff test value) respectively. When both K-S and GOF are greater than 0.5, the simulation results are good. The solid line represents the best geological thermal history path, the dotted line represents the better geological thermal history range, and the dotted line represents the acceptable geological thermal history range.
According to the parameters related to fission track and basic geological characteristics, the geological thermal history is simulated, and Ketchum (1999) annealing model and Monte Carlo method are adopted. The simulated temperature ranges from ~ 130℃ above the fission track annealing zone to the present surface temperature. According to the fission track age characteristics of the sample, the simulation start time is determined. The simulation results are shown in figure 1-4-3 1, and the best thermal history path is obtained for each sample (see thick line in the figure). The dashed area represents the better fitting area of inversion simulation, and the dashed area represents the acceptable thermal history range. Each icon shows the sample code, measured and simulated trajectory length, measured and simulated mixed age, and K-S test and GOF age fitting parameters. When the K-S value and GOF value are both greater than 0.5, it is generally considered that the simulation results are better.
The inversion simulation results of apatite fission track show a geothermal history of slow cooling (figure 1-4-3 1), which can be roughly divided into three stages: first, rapid cooling; The cooling rate slows down or even remains basically the same near 150 ~ 140 Ma; The rapid cooling starts from about 20Ma until the surface temperature. The rapid cooling characteristics of K77 (plagioclase granite porphyry) and K79 (dacite) samples related to mineralization and alteration are not obvious in 20 ~ 0ma. 150 ~ 140 Ma is just the boundary time of tectonic mineralization period.
The historical characteristics of geological heat are similar to those in Altai area. Zircon and apatite age values are completely within the Altai zircon age range. The tectonic stage is also basically consistent with Altai.
To sum up, it is considered that the Tuwu area has experienced a very similar evolution process with the Altai area, and has a very similar tectonic activity, mineralization and geothermal history. This may be related to their control by Siberian plate and Indosinian plate.
refer to
Chen Wenming, Qu Xiaoming. 2002. Host Rock and Deposit Geology of Tuwu-Yandong (Porphyry) Copper Deposit in East Tianshan Mountains, 2 1 Volume, No.4, 33 1 ~ 340 pages.
Chen Yuchuan, Wang, Tang Yanling, Zhou Ruhong, Wang, Li. 2003. Discussion on the related problems of mineralization in Tuwu-Yandong copper-copper ore field. Geology of mineral deposits, 22 (4): 334 ~ 344.
Ren Bingchen, Yang Xingke, Li, Chen Qiang. 2002. Intermediate-acid intrusive magmatism in the East Tianshan Mountains and its geodynamic significance. Northwest Geology, Volume 35, No.4, 4 1 ~ 64.
Qin, Fang Tonghui, Wang Shulai, Feng Yimin, Xiu Qunye. 2002. Study on tectonic division, evolution and metallogenic geological background of East Tianshan plate. Geology of Xinjiang, Volume 20, No.4, pp. 302-308.
Yang Xingke, Li, Wu. 2002. Metallogenic geological characteristics and deposit correlation of Tuwu super-large porphyry copper deposit in East Tianshan Mountains. Northwest Geology, Volume 35, No.3: 67 ~ 75.
Rui Zongyao, Wang Longsheng, Wang Yitian, Liu Yulin. 2002. Discussion on the Age of Tuwu and Yandong Porphyry Copper Deposits in East Tianshan Mountains. Geology of mineral deposits, 21(1):16 ~ 22.
Wang Futong, Feng Jing, Jiang, Zhang Zheng. Characteristics of Tuwu large porphyry copper deposit in Xinjiang and its discovery significance. Geology of China, 28 (1): 36 ~ 39, 25.
Zhang Lianchang, Qin, Ying Jifeng, Shu Jiansheng. 2004. Adakite in Tuwu-Yandong porphyry copper belt in East Tianshan and its relationship with mineralization. Acta petrolei sinica, 20 (2): 259 ~ 268.
Behrmans F, De Corte F, Vandenhaut P. 1994. Composition of glass doped with SRM and CN U: significance of being used as thermal neutron flux monitor in fission track detection. Radiation measurement, 24(2): 153~ 160
American mineralogist. Variability of apatite fission track annealing kinetics: Ⅲ. Extrapolated geological year: 1235~ 1255
Gleadow AJW, Duddy IR, Green PF and Loveling J.F.1986. Limited fission track length in apatite: a diagnostic tool for thermal history analysis [J]. Minerals and Petroleum, 94:405~4 15
Green postal code 1986. Thermotectonic evolution in northern England: evidence from fission track analysis, Geology, 5:493~506.
Hurford A.J. 1982 and Green P.F, User's Guide to Fission Track Dating and Calibration, Geoscience Newsletter, 59:343~354.
Late Paleozoic strike-slip shear zone in eastern Central Asia: new tectonic and geochronological data. Tectonics, 22(2): 1009
Simulation c, ArN Old no, cantagrare J m 1999. Earth science letter171:107 ~122
Xiao Weijun, Lichun Zhang, Qin Jianzhong, Sun, Li Jianlin. 2003. Paleozoic proliferation and collision structures in the East Tianshan Mountains: implications for the growth of the Central Asian continent. American Journal of Science, 304:370~395.
Xu Xinwei, Ma Tingnan, Sun Liqun, Cai Xinping. 2003. Characteristics and dynamic genesis of the large-scale Gyorotag ductile compression zone in the eastern Tianshan Mountains. Journal of structural geology, 25:1901~1915.
(Yuan Wanming, Bao Zengkuan, Dong Jinquan, Gao)