Figure
1.
Tectonic sketch of Dabie Mountains area, China. Ⅰ. north arc complex; Ⅱ. South Dabie collision complex; Ⅲ. Susong metamorphic cover.
| Citation: | Guxian Lü, Ruixun Liu, Fangzheng Wang, Jing Chen. Formation Depth of Coesite-Bearing Eclogite, Dabie UHPM Zone, China. Journal of Earth Science, 2004, 15(2): 206-215.
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The plastic deformation of garnet in coesite bearing eclogite, quartz eclogite and garnet amphibolite of the UHPM complex in Yingshan County in the Dabie Mountains has been studied. The stress generated by the strong tectonic movement was an important component of the total pressure that resulted in the formation of the eclogite in the Dabie UHPM zone. The three dimensional tectonic principal stresses and additional tectonic stress induced hydrostatic pressure [
In recent years, the research about the deep crust has become one of the frontier fields in earth sciences. The statement that the hydrostatic pressure is equal to the gravity value of the overlying rocks in studying a dynamic state of a certain underground site seems to have become a theoretical concept since Grubeenman and Niggle proposed that the temperature and pressure are positively proportional functions to the depth value in the crust.
Since the discovery of minor diamond and coesite inclusions in the garnet from metamorphic rocks (Xu et al., 1992), ultrahigh-pressure metamorphism (UHPM) has aroused a great interest of geologists. The chemical composition, zonation and snowball structure of the deformed garnet have been studied extensively, but no emphasis has been placed on the microstructure of deformed garnet. One of the reasons is that garnets are cubic and isotropic, and its ductile deformation is difficult to study with optical microscopy. Garnet has been long regarded as a mineral highly resistant to plastic deformation. Recent studies using the transmission electron microscopy (TEM) have changed this idea. Doukhan et al. (1994) studied the garnet from kimberlite and found that the dislocation density in the garnet may be as high as 1011/cm2 and is one order of magnitude lower than that in olivine when they are deformed under the same deformation conditions (Ando et al., 1993). Garnet is easy to be deformed at 900 ℃, but difficult at < 700 ℃, as suggested by Ji and Martignole (1994). Chen et al. (1996) studied the dislocation of the plastic deformation of the garnet of the Dabie eclogite, and successively calculated differential stresses during the main retrograde metamorphic stage.
Concerning the role of the tectonic force in the total hydrostatic pressure (Lü, 1995a, 1986, 1982; Lü and Kong, 1993), several scientists have proposed a new method for the calculation of the depth of petrogenesis and metallogenesis (Chen et al., 1995; Lü, 1995b, 1991a; Chen, 1993; Lü and Kong, 1993; Zhu and Ren, 1988). The reconstruction of the three-dimensional petrogenic principal stresses of coesite-bearing eclogite in the Dabie UHPM zone, following the formula and coefficients of differential stresses of plastically deformed garnet (Chen et al., 1995; Chen, 1995), suggested a new concept for the formation of the rocks occurring in the strongly compressive environment of the crust, with their formation depth measured, and then provided a new perspective of the tectonic physicochemical state and deep tectonic process about the UHPM (Lü, 1991b).
Some researchers advocate that the depth of gold mineralization in the gold deposits of Jiaodong, China ranges from 4 to 6 km. This depth was calculated with the W/SW (weight/special weight) method according to the pressures of 80-140 MPa. If this depth had been true, the main gold ore body should have been eroded (Lü, 1991a, b; Zhu and Ren, 1988).
New data of the formation depth of the deposits have been collected with our new method modified by 
To estimate the petrogenic and metallogenic depth, a new calculation method should be established, which may be called the method for the calculation of the formation depth corrected by structure (Lü, 1997, 1995b, 1991a, b; Chen et al., 1995; Chen, 1995; Hassan et al., 1995; Kozlovsky, 1989; Zhu and Ren, 1988; Le and Du, 1986; Wang et al., 1979; Murrell, 1976), i.e. the additional gravity-induced hydrostatic pressure pg should be obtained by the subtraction of the additional tectonic stress-induced pressure ps from the hydrostatic pressure field p, and then the depth with pg should be calculated and measured.
The data about the metamorphic rock-forming depth are, at present, obtained with the W/SW method with the pressure measured. The increasing attention has been paid to the Dabie-Sulu UHPM zone, where are exposed the eclogites with coesite and diamond inclusions related to the continent-continent collision-orogeny (Okay, 1993; Xu et al., 1992). These researches are important for our understanding of the genesis and metamorphic history of the eclogites, the orogenic process of the continent-continent collision and the tectonic evolution. But the method for the calculation of the depths of underthrusting-uplifting and their change shown by metamorphic minerals (Cong et al., 1995; Liou et al., 1995) needs to be further proved.
Experimental and theoretical studies have proved that diamond, coesite, omphacite and hornblende occur at 5.0-1.2 GPa (and at the corresponding temperatures). However, it does not mean that the formation pressure can be directly identified with the W/SW method, because the pressure is not derived only from the gravity of overlying rocks. Attention should be paid to the existence of the additional tectonic stress-induced hydrostatic pressure in the strong collisional orogenic environment, indicating explicitly that diamond and coesite in the Dabie tectonic-metamorphic zone are probably products of the intracrustal activity (Lü and Liu, 1996). As suggested by Ren (1994), the high and ultrahigh-pressure metamorphism during the Indosinian in the Qinling-Dabie area has already indicated three structural levels in the crust, the shallow (blueschist of the Wudang Mountains), the middle (blueschist of the Mulan Mountains in Hubei Province) and the deep (eclogite etc. in the Taihu area, Anhui Province), which represent the bottom of the sedimentary laccolith, the upper crust, and the deep crust or upper mantle, respectively. Therefore, the Mesozoic ultrahigh-high-pressure metamorphism in the Dabie area and East Qinling is not the product of downward thrusting of a deep-seated plate to the depths of 100-120 km, but that of the shear-slide movement in the deep levels of the crust. When the p and T conditions for the formation of ultrahigh-high-pressure minerals are calculated, the strong compresso-shear produced by tectonic dynamic force instead of the value of hydrostatic pressure should be employed to calculate their genetic depth.
The studied eclogite, about 3 km northeast of Yingshan County, Hubei Province (Fig. 1), is located in an ultrahigh-pressure metamorphic complex (Chen et al., 1996, 1995; Chen, 1995; Cong et al., 1995; Zhang et al., 1990). The metamorphic rocks in the studied area include feldspathic gneisses with minor coesite-bearing eclogites and amphibolite (Li et al., 1993). The coesite-bearing eclogites occur as lenses several centimeters to tens of meters in size surrounded by gneiss. There is no clear-cut boundary between the eclogites and the amphibolites. Petrographic study proved that the amphibolites were derived from the retrograded metamorphism of eclogites.
Some samples of coesite eclogite, quartz eclogite and garnet amphibolite were collected in order to study the ductile deformation of garnet during the retrogradation of eclogite to amphibolite. The compositions of garnets in the coesite eclogite (4A), quartz eclogite (3F) and garnet amphibolite (3C) are listed in Table 1.
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According to the petrological observation (Chen et al., 1996, 1995; Chen, 1995), three metamorphic stages, i.e. the coesite eclogite stage, quartz eclogite stage and retrograded amphibolite stage, can be recognized in the eclogites in the Yingshan area. Thecoesite eclogite stage is represented by the mineral assemblage of coesite inclusion+garnet+omphacite. The peak metamorphic p-T conditions were greater than 2.8 GPa (by using a Qz=Coes geobarometer (Mirwald and Massonne, 1980)) and (850±50) ℃ (by using a Grt-Cpx geothermometer (Powell, 1995)). The quartz eclogite stage is represented by garnet+amphibole+quartz. The metamorphic conditions in this stage were estimated at T= (750±50) ℃ and p=1.4-1.5 GPa by employing the jadeite content (Xjd=37.7 % to 41.3 %) in omphacite (Holland, 1980) and the garnet-dinopyrocene geothermometers. The retrograded amphibolite stage is represented by the assemblage of amphibole+plagioclase+garnet. The metamorphic p-T conditions were estimated at about 0.9 GPa and (530±50) ℃ obtained with a geothermobarometer (Blundy and Holland, 1990; Hollost et al., 1987). In summary, the Yingshan eclogites experienced a clockwise p-T path and a dynamic change from ultrahigh and high pressure to medium-low pressure.
Coesite eclogite (4A) : free dislocations and a few dislocation networks are developed in garnet (Fig. 2a). The free dislocation density is as high as 1×108/cm2.
Quartz eclogite (3F) : the microstructures in garnets of the quartz eclogite include free dislocations, tiltwalls, complex dislocation networks and subgrains of garnet (Fig. 2b, 2c). The free dislocation density (6.2×107/cm2) is lower than that in coesite eclogite. Subgrain boundaries are composed of dislocation arrays and dislocation networks, which are formed by slipping and climbing of dislocations.
Garnet amphibolite (3C) : the dislocation tangle is observed only in garnet amphibolite. The dislocation density (2.2×108/cm2) is higher than those in coesite eclogite and quartz eclogite. Dislocation tiltwalls and complex dislocation networks (Fig. 2d) have not been observed (Table 2).
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For many metals and minerals, a relationship between the dislocation density and applied stress are described as
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where α is the material coefficient; κ is constant; σ is the differential stress; μ is the shear modules; ρ is the dislocation density, and b is Burgers vector (Twiss, 1977). De Bresser (1991) suggested κ=2 and α=1.172 (log (2α) =ca. 0.37) for olivine, quartz and calcite. However, the value of the material coefficient always gives a smaller estimation of paleostress for garnet. When the material coefficient value (α=1.172) was used to calculate differential stresses (Ando et al., 1993), different values of differential stresses in the same garnet peridotite were obtained by Ando et al. (1993). This contradiction indicates that the material constant (α) is not the same for different materials. Therefore, it is suggested that an experimental coefficient value, α=2.5 (Chen et al., 1995; Chen, 1995), is used as the revised value for garnet. The differential stress obtained by revision of the material coefficient value α of garnet is close to that from olivine (Table 3).
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Based on this formula and the revised material coefficient, the differential stresses of garnets were measured in coesite eclogite, quartz eclogite and garnet amphibolite of the Dabie UHPM zone (Table 4).
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Three metamorphic stages of the studied eclogite have been recognized, i. e. the coesite eclogite stage, quartz eclogite stage and retrograded amphibolite stage (Chen et al., 1996; Chen, 1995). The microstructures of garnets from coesite eclogite, quartz eclogite and garnet amphibolite record the plastic-flow rheology of different metamorphic stages (Twiss, 1977). The above-mentioned data seem to record a response of the dislocation structure of garnet to the p-T-D paths of eclogite (Fig. 3). The higher dislocation density (1×108/cm2) and the great differential stress (0.5 GPa) are recorded in garnet from coesite eclogite. The upper crust material is generally considered to have been carried rapidly down to the depth of 90 km and to have suffered UHPM, indicating that those rocks experienced a rapid increase not only in lithostatic pressure (and temperature) due to increasing gravity of overlying rocks, but also in large differential stress and additional tectonic hydrostatic pressure resulting from structural compression.
For this reason, the formation and variation depths of rocks after the additional tectonic hydrostatic pressure is eliminated are obviously shallower than those estimated with the W/SW method.
The measured and observed samples were chosen from the above-mentioned samples (Chen et al., 1996, 1995; Chen, 1995). This kind of rock is characterized by the mineral association of coesite inclusion+garnet+omphacite, and the garnet shows clear plastic deformation (Fig. 4a). The plastically deformed garnet and clinopyroxene are oriented (Fig. 4b). The relict clinopyroxene in garnet has a prograde metamorphic texture (Fig. 4c). The garnet shows plastic and oblong deformation. The coesite and special "dilating-cracking fissures" occur in plastically deformed garnet (Fig. 4d). The peak metamorphic stage was marked by the p-T conditions of p≥2.8 GPa, T= (850±50) ℃.
In order to obtain the correct data, measured minerals were chosen by an electron microprobe. Two groups of samples were used, of which sample Y1 was the most representative after thin sections and electron microscopy films are both prepared.
The ratios of deformed garnet in the case of a > b > c are α1=b/c, α2=a/b, α3=a/c. The ac and bc planes containing the principal deformation axes were chosen. Two sections perpendicular to each other were cut and prepared, and the deformation ratios, especially α3=a/c for calculation were measured under the microscope (Fig. 5).
The ratios of deformation axes of garnet are listed in Table 5.
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The free dislocation density D in deformed garnet was observed under the electron microscope and A value (in the ac plane) and B value (in the bc plane) of differential stresses were calculated according to equation (1) (Table 6).
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Let the ratios between plastic strain and general strain be equal in ac and bc planes. When ε1=εe1+εp1 and ε3=εe3+εp3, and if εp > > εe, given ε1/ε3=εp1/εp3, then εp1/ε1=εp3/ε3. Following the equation system (2)
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the values of three principal stresses that cause residual (i. e. plastic) deformation may have been obtained (Lü, 1997, 1995a, b, 1991a, b, 1982; Chen et al., 1995; Chen, 1995; Lü and Kong, 1993; Zhu and Ren, 1988; Le and Du, 1986; Wang et al., 1979). Because the additional tectonic hydrostatic pressure psis equal to an unchanged quantity (Wang et al., 1979), the same psvalues are derived from the calculation of the stress values measured in both principal planes and non-principal planes of strain. The calculated results are shown in Table 7.
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p≥2.8 GPa is estimated by coesite contained in deformed garnet. This study takes the average specific weight of the crustal rocks as 2.7 g/cm3 (26.478×105 Pa). The study (Lü, 1995a, b, 1986; Lü and Kong, 1993) shows that only a part of gravity can be transformed into the isotropic normal stress called the additional gravity hydrostatic pressure pg, and a transformation coefficient is (1+υ) /[3 (1-υ) ] obtained on the basis of Terzaghi's hypothesis (Le and Du, 1986) and the structural phenomena are observed in the superdeep drill hole at Kola (Kozlovsky, 1989). If υ=0.25 and the specific weight of rocks is 2.7 g/cm3, then the rock column, 100 m long, produces the hydrostatic pressure p'g=14.711×105 Pa only. Therefore, if the remaining value minus ps from p is considered as the gravity additional hydrostatic pressure pg, the petrogenic depth H, i. e. the thickness of the overlying rocks, should be obtained by dividing pg by p'g=14.711×105 Pa. The calculated results are listed in Table 8.
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(1) Tectonism not only deforms the rocks in shape, but also changes their volumes. The latter is caused by the isotropic compressive (tensile) stress tensor, called the additional tectonic stress-induced hydrostatic pressure, expressed as ps. There are various ps values in different structural deformation zones at the same depth.
(2) The total hydrostatic pressure at a point in the crust is a combination of two isotropic stresses, the additional tectonic hydrostatic pressure ps and the additional gravity-induced (or gravity) hydrostatic pressure pg. Therefore, the depth data thus collected will be more accurate, if we first calculate pg by the subtraction of ps from p, and then use the remnant pg to calculate the thickness of overlying rocks or the petrogenic depth. This method is called the method for the calculation of the petrogenic and metallogenic depth corrected by structure.
(3) Besides the greater burial depth, the Dabie UHPM zone experienced great tectonic differential stress and additional tectonic hydrostatic pressure. The garnet in eclogite of Yingshan County, Hubei Province, in the Dabie area, shows obvious plastic deformation. An analysis of dislocation and deformation shows that the deviated stress field and differential stress of the main retrograde metamorphic stage can be recovered.
Both the deformation measurements and the stress field recovery can be used to obtain the 3-D principal stresses and additional tectonic hydrostatic pressure. The structure-corrected formation depth of coesite-bearing eclogite is ≥32.09-32.11 km, which is different from the depth (over 100 km) calculated with the W/SW method.
(4) The study and calculation of an "additional tectonic stress-induced hydrostatic pressure" have important significance in the combination of both the branch of structures and textures of the crustal material and the branch of its composition. Therefore, a new concept is created of the relation between the structural state and physicochemical process in the deep levels of the crust, providing a new basis for the determination of the physicochemical state during the formation of rocks and minerals.
This study modifies the concept that the hydrostatic pressure value is equal to the gravity value of the overlying rocks, and gives a new method for the study and calculation of the formation depth of geological bodies.
(5) Generally speaking, the ultrahigh-high-pressure metamorphic zone, in which there occur ultrahigh-high-pressure metamorphic minerals, diamond coesite, etc., is considered to have been carried to very deep levels by plate subduction and then to have exhumed to the surface when the zone attained ultrahigh-highp-T metamorphism. But this study shows that the ultrahigh-high pressure metamorphism may have taken place only at a depth of about over 30 km in the crust. The ps was generated by the strong tectonic compression between the North China block and South China block, and then it was superimposed on the pg. The combined pressure produced the ultrahigh-high conditions which, especially when p≥2.8 GPa, caused the facies change of rocks, i. e. the ultrahigh-high-pressure metamorphic rocks are the product of the tectonic physicochemical environment (Lü and Liu, 1996; Ren, 1994; Lü, 1991b, 1986).
(6) Although the calculation of differential stresses of naturally deformed minerals based on the dislocation density has aroused interests among geologists, there are some problems in this method. The accuracy in the calculation might decrease because ① the distribution of dislocations is inhomogeneous; ② the dislocation density changes from crystal plane to crystal plane, and ③ the constant κ (Table 3) calculated in the experiments differs from that in naturally deformed rocks. Therefore, these estimations should serve only as reference values, rather than accurate ones.
Besides, the strain-stress formula and its assumed conditions of plastic deformation established by the authors need to be further perfected, and the sample measurements are short of systematization and accuracy; therefore, the data on the depth of coesite-bearing eclogite are for reference only.
Although there are many problems mentioned above in the research, the method for the calculation of the structure-corrected petrogenic and metallogenic depth is superior to the W/SW method not only in the research conception but also in the data reliability and accuracy.
ACKNOWLEDGMENTS: We would like to express our thanks to Guo Wenkui, Song Shuhe, Li Tingdong, Ma Zongjin, Zhang Bingxi, Ouyang Ziyuan, Ye Danian, Ren Jishun, Shen Qihan, Chang Yinfo, Zhai Yusheng and Wang Dezi for their discussions and helps in the research. Thanks are offered to our tutors Yang Kaiqing, Chen Qingxuan and Sun Dianqing, to Zhang Bingxi, Ma Zongjin, Li Tingdong and Ren Jishun for their discussions and critical reviews, and to Shao Liqin, Ma Hongjian and Ye Yujiang of the State Science and Technology Committee, China and to Chen Xiaoning, and Luo Yuanhua of the State Planning Commission, China for their supports. This work is now supported by the Major Science and Technology Development Program (No.2002201) and the Geologic Survey Subject (200110200104) of the Ministry of Land and Resources, and also by the State Science and Technology Committee (KG-1994-83), the State Planning Commission of China (JG947110) and the National Natural Science Foundation of China (No.49572149).| Ando, J. I., Fujino, K., Tadeshita, T., 1993. Dislocation Microstructures inNaturally Deformed Silicate Garnets. Physics of the Earth and Planetary Interiors, 80: 105-116 doi: 10.1016/0031-9201(93)90041-7 |
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Guxian Lü, Ruixun Liu, Fangzheng Wang, Jing Chen. Formation Depth of Coesite-Bearing Eclogite, Dabie UHPM Zone, China. Journal of Earth Science, 2004, 15(2): 206-215.
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