东天山地区金矿床成矿流体地球化学及其成矿机制

The mechanism of gold ore formation in the eastern Tianshan Mountains, Xinjiang Uygur Autonomous Region, that has been dealt with from various aspects, remains unclear. On the basis of investigations of regional geology, ore deposit geology, and microscopic observations of ores and related rocks of the Jinwozi, the 210, and the Mazhuangshan gold ore deposits, this thesis made a systematic research on the microthermometry of gangue quartz-hosted fluid inclusions, gas, liquid ion and rare earth element compositions and hydrogen, oxygen isotope compositions of sulfide- and quartz-hosted fluid inclusions, and sulfur and lead isotope compositions of sulfide ore minerals from the major ores in the three deposits. On the basis of the above synthetic studies, sources of ore-forming fluids and metals, and mechanism of gold ore formation in the region were discussed. Gas compositions of pyrite- and sphalerite-hosted fluid inclusions were first analyzed in this thesis. Compared with gangue quartz-hosted fluid inclusions, the sulfide-hosted ones are richer in gaseous species CO2, CO, and CH4 etc. Both gas and liquid CO2 are commonly observed in fluid inclusions, whereas halite daughter minerals rarely occur. Ore-forming fluids for the three gold ore deposits are characteristically of medium to low temperatures, medium to low salinities, are rich in CO2 and Na+, K+, Cl" ions. Gas covariation diagrams exhibit linear trends that are interpreted as reflecting mixing between the magamtic fluid and meteoric-derived groundwater. Regarding rare earth element compositions, the Jinwozi and the 210 deposits show moderate to strong LREE/HREE fractionations with negative Eu anomalies. However, the Mazhuangshan deposit shows little LREE/HREE fractionation with positive Eu anomalies. Hydrogen and oxygen isotope compositions of pyrite-hosted fluid inclusions that were first analyzed in this thesis indicate the presence of magmatic water. Hydrogen and oxygen isotope compositions of pyrite- and quartz-hosted fluid inclusions suggest mixing between magmatic water and meteoric-derived groundwater. Sulfur and lead isotope compositions of sulfide ore minerals indicate multi-sources for the metallogenetic materials that range from the crust to the mantle. On the basis of the above synthetic studies, genesis of the gold ore deposits in the eastern Tianshan Mountains was approached. From the Middle-Late Hercynian to Early Indosinian, geodynamic regime of the region was changing from the collisional compression to the post-collisional extension. During the period, magmas were derived from the crust and the mantle and carried metallogenetic materials. Magma intrusion in the upper crust released the magmatic fluids, and drove circulation of groundwater. Mixing of magmatic fluid with groundwater, and extraction of metallogenetic materials from the country rocks are the mechanism for the gold ore formation in the eastern Tianshan Mountains.

东大别山晚中生代主剪切带及伸展构造研究

Dabie shan lies between Northchina crust and Yangzi crust, which is the result of the collisional orogenen in Triassic period. The biggest area of UHP metamorphic zone have been found in Dabie Shan, which have been verified formed during the course of collision and extrusion after orogenic activity. The Dabie shan is divisioned into four parts, which are North Huaiyang metamorphic zone, North Dabie complex zone, South Dabie ultra-high pressure metamorphic zone and Susong metamorphic zone. Extension structure of late Mesozoic is the key to explain the intrusion and outcrop of UHP metamorphic rocks in Dabie Shan. During the course of structure evolution of the Dabie shan in late Mesozoic period, Luotian dome was formed with the old gneiss lifting from the core of the Dabie shan. There are four enormous ductile zone circled Luotian dorm. Xiaotian-mozitan shear zone is the limit of North Huaiyang metamorphic zone and North Dabie complex zone; Shuihou-wuhe shear zone is the limit of North Dabie complex zone and South Dabie ultra-high pressure metamorphic zone; Taihu-mamiao shears zone is the limit of South Dabie ultra-high pressure metamorphic zone and Susong metamorphic zone and Susong-Qingshuihe shear zone is the south limit of Susong metamorphic zone; the old stress at Dabie shan in late Mesozoic was about 90MPa through the experiment of transmission electricity microscope. The main four ductile shear zone of Dabie shan all have the characteristic of detachment, Xiaotian-mozitan shear zone detached to NNE, the detachment direction of Shuihou-wuhe shear zone and Taihu-mamiao shears zone is SSE, and Susong-Qingshuihe shear zone is SW. The finite strain measurement show that Xiaotian-mozitan shear zone have experienced detachment which was more than 50km, and the detachment of Susong-Qingshuihe shear zone was more than 12km in late Mesozoic; the Flin parameter of Shuihou-wuhe shear zone is much smaller than 1(0.01-0.1), which show that this shear zone was squeezed when it was formed and the initiative function of Luotian granite intrusion during the course of detachment. The Flin parameter of Taihu-mamiao shears zone is above 1(1.1) and Susong-Qingshuihe shear zone is much more than 1(7.6), which show that they are formed in the state of extension at the beginning. These all Flin parameter imply a transition from pure shear to simple shear of the south three shear zone circling Luotian dome from north to south. The rock group analysis show that the rocks inside shear zone encountered middle or high temperature metamorphic activity. The single mineral ~(40)Ar/~(39)Ar age of the main shear zone at Dabie shan show that the three shear zone north to Luotian dome were formed about 190Ma.Taihu-mamiao shear zone was the earliest, Susong shear zone was later than former, and Shuihou-wuhe sheanaone was the latest. They were all the chanel of returning of UHP metamorphic rocks, so they all representative the returning age of UHP metamorphic rocks. The final outcrop of these UHP metamorphic rocks was due to the detachment aroused by the enormous magma intrusion. The biotite age of deformed rocks in Susong-Qingshuihe shear zone is in average 126Ma, and the age of Xiaotian-mozitan is about 125Ma, which is in the same time or a little later than magma intrusion of Luotian dome, and imply that granite intrusion of late Mesozoic in Dabie orogenen is the reason of the detachment.

东海榴辉岩向斜长角闪岩的转化过程

The Ultrahigh Pressure Metamorphic (UHPM) eclogite, which was resulted from deep subduction of crustal continent, is very significant due to its continental dynamic implications. Further more, this kind of rocks experienced great P-T, fluid and stresses changes during its forming and exhumation, causing mineral reactions occur intensively, which resulted in a lot of fantastic micro-texture. The micro-texture was preserved duo to a rapid exhumation of the eclogite. This PhD dissertation takes such micro-textures in 10 Donghai eclogite samples South Sulu UHPM terrene, as research object to reveal the transformation of the eclogite to amphibolite. Microscope and Scanning Electron Microscope were employed to observe the micro-texture. Basing on microprobe analysis of minerals, the ACF projections and iso-con analysis were used to uncover the mineral reactions during the transformation. Micro-texture observation (both of Microcopy and Electron Scanning Microscope), demonstrated: l.The peak mineral assemblage of the researched Donghai eclogites is garnet + omphacite + rutile (+ kyanite + aptite +coesite). 2.The transformation of the Donghai eclogite to amphibolite can be divided into two stages: The earlier one is Symplectization, resulting in the forming of diopside + albite (+magnetite) symplectite that occurred only along the boundary between two adjacent omphacite grains. Other minerals were not involved in such reaction. The latter stage is Fluid-Infiltration of the eclogite, which was caused by fluid-intrusion. The infiltration is demonstrated by amphibolization of the symplectite, decomposition of garnet and the forming of some hydrous minerals such as phengite and epidote, and resulted in an amphibole + plagioclase + phengite + epidote or ziosite assemblage. Basing on microprobe analysis of the minerals, ACF projections indicated: In the ACF diagrams, the two joint lines of peak Grt + Omp and Dio + Ab crossed at Omp projection-point, indicating that the garnet had not taken part in the forming reaction of the Dio + Ab symplectite, just like that had been pointed out by micro-texture observation. In the ACF diagrams, the hornblende + plagioclase + epidote + phengite quadrilateral intersected with Dio + Ab + Grt triangle, demonstrating that the hydrous mineral assemblage was formed by fluid infiltration through garnet, diopside and albite. Iso-con (mass-balance) analysis of the symplectization and infiltration reveals: 1.The symplectization of the omphacite has a very complex mass exchange: Some symplectite gained only silicon from its surroundings; and some one requires Ca, but provides Na to its surroundings; while other symplectite provides Ca, Mg and Fe to its surroundings. 2.The infiltration cause variable mass exchanges occurring among the garnet, diopside and albite: In some eclogite sample, no mass, except H2O, exchange occurred during the infiltration. Meanwhile, there was not any hydrous mineral except hornblende formed in the sample accordingly. In some samples, the mass exchange among the three minerals is complex: amphibolization of the diopside in a symplectite gained Al from garnet, and provided Si and Ca to its surrounding, resulting in a Si, Ca and Al-rich fluid. Correspondingly, there was a lot of phengite and ziosite occurred in the sample. In other samples, the amphibolization of a symplectite provided Fe and Mg besides Si and Ca to its surrounding while gained Al. In such kind of sample, epidote occurred within the hydrous mineral assemblage. Synthesizing the micro-texture observation, ACF analysis and iso-con analysis, we deduced the transformation procedure as following: 1. A symplectite after an omphacite was resulted by one, or two, or all of following mineral reactions together: Jd (Ca-Tsch) +SiO2=Ab (An) (1) 4NaA IS i.A+CaO=2NaAlS i308+Na20+CaAl2S 1208 (2) 2NaAlSi2OB (Jd in Omp)+CaMgSi;,0B(Dio in Omp)-2NaAlSi:,O"(Ab)+Ca0+Mg0 (3) 2(CaAl2Si0fi) (Ca-tsch in Omp)+CaFeSi2O6(Hed in 0mp)-H>2CaAl2Si208(An)+Ca0 + FeO (4) A CO2-rich fluid is suggested as cataclysm for the above reactions, which largely increased the mobility of Ca, Mg and Na resulted from reaction (2), (3) and (4). The immobile product Fe2* combined with rutile to form ilmenite, resulting in rutile + ilmenite symplectite. Or, the Fe was precipitated as hematite locally. A procedure of the fluid infiltration as following is suggested: I .A hydrous fluid intruded into the eclogite, and reacted first with garnet to form hornblende and extra Al, resulting in a hornblende film around the garnet grain and an Al-rich fluid. 2.The Al-rich fluid infiltrated through the symplectite, OH" and part of the Al in the fluid combined with Dio while some Si and Ca in the Dio were dissolved made the Dio transferred to amphibole. Meanwhile, plagioclase-type cation exchange occurred between the fluid and plagioclase in the symplectite, making the plagioclase have a higher An-content. 3.Above infiltration and cation exchange resulted in an Al, Si, Ca (and K, providing the primary hydrous fluid contain K)-rich fluid. 4.Under suitable conditions, the solute in the fluid precipitated to form phengite firstly. After the K element in the fluid was consumed up, ziosite or epidote was formed. If the fluid did not contain any K. element, only ziosite or epidote was precipitated. For those eclogites, where all omphacite had been replaced by symplectite before infiltration, neither element exchange occurred, nor did phengite or epidote form during the infiltration. At the last stage, the garnet was oxidized and breakdown: garnet + H2O = epidote + hornblende + hematite, due to more and more fluid intruding into the eclogite. At this time, all the peak minerals were replaced by amphibolite-phase ones, and the eclogite transformed to an amphibolite completely. Tentative pressure calculation indicates that the infiltration occurred at 3-6kbar (about 10-20km depth), where the deformation mechanics transformed from brittle to ductile yield. At such depth, the surface water can permeate the rocks through fault system, causing a rapid cooling.

矾山杂岩体成因及其与磷（铁）矿的成矿关系

The Fanshan complex consists of layered potassic ultramafic-syenite intrusions. The Fanshan apatite (-magnetite) deposit occurs in the Fanshan complex, and is an important style of phosphorus deposit in China. The Fanshan complex consists of three (First- to Third-) Phases of intrusion, and then the dikes. The First-Phase Intrusive contains ten typical layered rocks: clinopyroxenite, biotite clinopyroxenite, coarse-grained biotite clinopyroxenite, pegmatitic orthoclase-biotite clinopyroxenite, variegated orthoclase clinopyroxenite, interstitial orthoclase clinopyroxenite, biotite rock, biotite-apatite rock, biotite rock and magnetite-apatite rock. This layered intrusive consists of nine rhythmic units. Each rhythmic unit essentially comprises a pair of layers: clinopyroxenite at the bottom and biotite clinopyroxenite at the top. The apatite (-magnetite) deposit is situated near the top of rhythmic Unit no. 6 of the First-Phase Intrusive. The Second-Phase Intrusive contains three typical rocks: coarse-grained orthoclase clinopyroxenite, . coarse-grained salite syenite and schorlomite-salite syenite. The Third-Phase Intrusive includes pseudo-trachytic salite syenite, porphyritic augite syenite, fine-grained orthoclase clinopyroxenite and fine-grained salite syenite. The origin of the Fanshan complex is always paid attention to it in China. Because most layered igneous intrusion in the world not only have important deposit in it, but also carry many useful information for studying the formation of the intrusion and the evolvement of magma. Two sketch maps were drawn through orebodies along no. 25 cross-cut on 425 mL and no. 1 cross-cut on 491 mL in the Fanshan mine. Through this mapping, a small-scaled rhythmic layering (called sub-rhythmic layering in the present study) was newly found at the top of the rhythmic Unit no. 6. The concept of sub-rhythmic layering is defined in this article. The sub-rhythmic layering is recognized throughout this apatite-rich part, except for magnetite-apatite rock. Presence of the layered magnetite-apatite rock is one of the characteristics of the Fanshan apatite (-magnetite) deposit. Thus, from this layer downwards six units of sub-rhythmic layering are recognized in the present study. Each unit consists of biotite clinopyroxenite (or biotite rock and biotite-apatite rock) layer at the bottom and apatite rock layer at the top. To study this feature in detail is an important work for understanding the origin of the Fanshan complex and apatite (-magnetite) deposit. The origin of the Fanshan complex and the relation of the formation of the apatite(-magnetite)deposit will be interpreted by the study of sub-rhythmic layering on the basis of previous research works. The magma formed the Fanshan complex was rich in K2O, early crystallized pyroxene, and after this phase more biotite crystallized, but no amphibole appeared. This indicated that the activity of H2O in the magma was low. Major element compositions of biotite and clinopyroxene (on thin sections) in the sub-rhythmic layering were analyzed using electron microprobe analyzer. The analytical results indicate Mg/(Mg+Fe*+Mn) atomic ratios (Fe*, total iron) of these two minerals rhythmically changed in sub-rhythmic layering. The trends of Mg/(Mg+Fe*+Mn) atomic ratio (Fe*, total iron) of biotite and clinopyroxene indicate that the magma evolved markedly from relatively magnesian bottom layer to less magnesian top layer in each sub-rhythmic unit. A general trend through the sub-rhythmic layering sequence is both minerals becoming relatively magnesian upwards. The formation temperatures for sub-rhythmic layering yield values between 600 and 800 ℃, were calculated using the ratio of Mg/(Mg+Fe+Mn) in the salite and biotite assemblage. The equilibrium pressures in the rhythmic layers calculated using the contents of Al in the salite were plotted in the section map, shown a concave curve. This indicates that the magma formed the First-Phase Intrusive crystallized by two vis-a-vis ways, from its bottom and top to its centre, and the magnetite-apatite rock was crytallized in the latest stage. The values of equilibrium pressures in the sub-rhythmic layering were 3.6-6.8(xlO8) Pa with calculated using the contents of Al in the salite. The characteristics of geochemistry in various intrusive rocks and the rocks or apatite of sub-rhythmic layers indicated that the Fanshan complex formed by the comagmatic crystallization. The contents of immiscible elements and REEs of apatite rock at the top of one sub-rhythmic unit are more than biotite clinopyroxenite at the bottom. The contents of immiscible elements and REEs of apatite of biotite clinopyroxenite at the bottom of one sub-rhythmic unit are higher than apatite rock at the top. The curves of rocks (or apatite) in the upper sub-rhythmic units are between two curves of the below sub-rhythmic unit in the primitive mantle-normalized trace element abundance spider diagram and the primitive mantle-normalized REE pattern. The trend for the contents of immiscible elements and REEs inclines to the same contents from the bottom to the top in sub-rhythmic layering. These characteristics of geochemistry of rocks or apatites from sub-rhythmic layering indicate that the latter sub-rhythmic unit was produced by the residual magma after crystallization of the previous sub-rhythmic unit. The characteristics of petrology, petrochemistry, geochemistry in the Fanshan complex and sub-rhythmic layers and the trends of Mg/(Mg+Fe+Mn) atomic ratio of biotite and clinopyroxene in sub-rhytmic layering rejected the hypotheses, such as magma immiscibility, ravitational settling and multiple and pulse supplement of magma. The hypothesis of differentiation by crystallization lacks of evidences of field and excludes by this study. On the base of the trends of formation temperatures and pressures, the characteristics of petrology, petrochemistry, geochemistry for the Fanshan complex and the characteristics of geochemistry for the rocks (or apatites), the trends of Mg/(Mg+Fe+Mn) atomic ratio of biotite and clinopyroxene in sub-rhytmic layering, and the data of oxygen, hydrogen, strontium and neodymium isotopes, this study suggests that the magma formed the Fanshan complex was formed by low degree partial melting of mantle at a low activity of H2O, and went through the differentiation at the depth of mantle, then multiply intruded and crystallized. The rhythmic layers of the First-Phase Intrusive formed by the magma fractional crystallized in two vis-a-vis ways, from the bottom and top to the centre in-situ fractional crystallization. The apatite (-magnetite) deposit of the Fanshan complex occurs in sub-rhythmic layering sequence. The the origin of the sub-rhythmic layering is substantially the origin of the Fanshan apatite (-magnetite) deposit. The magma formed the rhythmic layers of First-Phase Intrusive was rich in H2O, F and P at the later stage of its in-situ fractional crystallization. The Fanshan apatite (-magnetite) deposit was formed by this residual magma in-situ fractional crystallization. The magnetite-apatite rock was crystallized by two vis-a-vis ways at the latest stage in-situ fractional crystallization in the rhythmic layers. The result was light apatite layer below heavy the magnetite-apatite layer, formed an "inversion" phenomenon.

Mantle-derived gaseous components in ore-forming fluids of the Xiangshan uranium

The Xiangshan U deposit, the largest hydrothermal U deposit in China, is hosted in late Jurassic felsic volcanic rocks although the U mineralization post dates the volcanics by at least 20 Ma. The mineralization coincides with intrusion of local mantle-derived mafic dykes formed during Cretaceous crustal extension in South China. Ore-forming fluids are rich in CO2, and U in the fluid is thought to have been dissolved in the form of UO2 (CO3)22− and UO2 (CO3) 34− complexes. This paper provides He and Ar isotope data of fluid inclusions in pyrites and C isotope data of calcites associated with U mineralization (pitchblende) in the Xiangshan U deposit. He isotopic compositions range between 0.1 and 2.0Ra (where Ra is the 3He/4He ratio of air=1.39×10−6) and correlates with 40Ar/36Ar; although there is potential for significant 3He production via 6Li(n,α)3H(β)3He reactions in a U deposit (due to abundant neutrons), nucleogenic production cannot account for either the 3He concentration in these fluids, nor the correlations between He and Ar isotopic compositions. It is more likely that the high 3He/4He ratios represent trapped mantle-derived gases. A mantle origin for the volatiles of Xiangshan is consistent with the δ13C values of calcites, which vary from −3.5‰ to −7.7‰, overlapping the range of mantle CO2. The He, Ar and CO2 characteristics of the ore-forming fluids responsible for the deposit are consistent with mixing between 3He- and CO2-rich mantle-derived fluids and CO2-poor meteoric fluids. These fluids were likely produced during Cretaceous extension and dyke intrusion which permitted mantle-derived CO2 to migrate upward and remobilize U from the acid volcanic source rocks, resulting in the formation of the U deposit. Subsequent decay of U within the fluid inclusions has reduced the 3He/4He ratio, and variations in U/3He result in the range in 3He/4He observed with U/3He ratios in the range 5–17×103 likely corresponding to U concentrations in the fluids b0.2 ppm.

甘肃金川II号岩体岩浆演化及铜镍硫化物成矿过程探讨

金川矿床是超大型岩浆 Ni-Cu-PGE 硫化物矿床，它赋存有世界第三的镍储量（5.45×106 t，Ni 的平均品位为 1.2%）。该矿床位于华北板块西侧阿拉善地块西南边缘龙首山隆起中。本论文以金川矿区的 II 号岩体为研究对象，在系统整理前人工作的基础上，通过深入细致的野外地质考察和系统采样，选取有代表性的样品，进行详细的显微镜鉴定，并运用元素地球化学等手段，对 II 号岩体的源区特征、岩浆演化过程及其赋存的⑴、⑵号矿体的成矿机制等主要矿床学问题进行了系统成因研究，并尝试提出了二次硫化物熔离成矿模式。本论文主要取得以下几点结论性成果： 1）岩浆起源：起源于上地幔尖晶石－石榴石二辉橄榄岩过渡地带的下部。通过上地幔源岩的柱状部分熔融模式（≥25%）或三角部分熔融模式（10～15%），形成富PGE的S不饱和原始岩浆。 2）地壳同化混染：地壳物质的同化混染主要是由早期下地壳物质的同化混染和晚期上地壳物质的同化混染组成的多阶段同化混染，并且其成分为富钙质围岩。 3）结晶分异演化：金川II号岩体作为橄榄石堆积相，其橄榄石的结晶主要发生在上地壳深部岩浆房，而橄榄石与熔浆的反应及辉石和斜长石的结晶则主要发生在浅部岩浆房，既现今岩体所在位置。 4）S 的饱和机制：岩浆通道内下地壳物质的同化混染，导致岩浆硫饱和，并于岩浆通道中发生了第一次硫化物熔离；上地壳深部岩浆房中地壳物质的同化混染和橄榄石的分离结晶，促使硫饱和的母岩浆发生了第二次硫化物熔离。 5）深部岩浆房的演化：上地壳深部岩浆房中橄榄石分离结晶与硫化物熔离之后，在重力分异作用下，形成了自上而下的硅酸盐岩浆、橄榄石“晶粥”、含硫化物熔体的橄榄石“晶粥”以及矿浆的四层分层格局。同时，底部部分硫化物熔体发生了Pt合金（Pt-Fe）的脱离。 6）侵入期次：上地壳深部岩浆房中，母岩浆分异演化早期，其顶部含有尚未完全成长橄榄石颗粒的“晶粥”在构造应力挤压下首先上侵、成岩形成金川II号岩体顶部、呈“上悬体”的中细粒含辉橄榄岩；分层格局形成之后，橄榄石“晶 VI 粥”、含硫化物熔体的橄榄石“晶粥”以及矿浆依次上侵成岩、成矿，分别形成金川 II 号岩体上部的二辉橄榄岩相、⑴、⑵号矿体的主体以及⑵号矿体底部的块状矿石。

学习不良少年的污名效应研究

Stigma is defined as a sign of disgrace or discredit that sets a person apart from others. Stigmatized individuals had been significantly influenced by their group-based stigma. Through the methods of laboratory experiment and questionnaire surveys, the current study started with examining the attitudes of middle school students to the students with learning disabilities (LD), systemly explored the characteristics of perceived stigma and self-stigma of LD students, the mechanism that the influences of stigma on students with LD, and the mental control required to cope with the stigma. The results of the present studies had significant implications for the understanding of the LD phenomenon and the intervention of LD adolescents. The results indicate that: 1. Generally, middle school students had negative implicit attitude and negative explicit attitudes towards the LD students. The effect size of the phenomenon of this study is large. The LD students showed a more positive attitude than others on the explicit attitude measure; all students consistently had negative attitudes toward LD students on the implicit attitude indices, in addition, no group differences and gender differences were observed in the implicit attitude. 2. Eight hundred and seventy two students were surveyed to test the reliability and validity of the new developed perceived stigma scale and self-stigma scale. Both questionnaires showed sufficient content validity, construct validity, criterion-related validity and adequate internal consistency reliability. Then, both questionnaires were administered to student with high academic achievement (high achiever), students with middle academic achievement (middle achiever), and LD students. Results revealed that the LD students mildly stigmatized by the social culture. The LD students had more stigma perception and self-stigma than the middle achievers and high achievers. The results also indicated that there were more stigma perception and self-stigma for LD students in grade two than that of LD students in grade one and grade three; meanwhile, male LDstudent hade more stigma perception and self-stigma than female LD students in all grades. 3. A latent variable path analysis was conducted to investigate how the stigma affect the academic goals using the data collected from 186 LD students. The results suggested that the LD-related stigma did not have direct influence on academic goals. The LD-related stigma indirectly influenced the academic goals through mediating effects of self-stigma and academic efficacy. 4. Stereotype threat could have some influences on the relationship between the task feedback and self-esteem. The results of study using eighty-four LD students showed that: when the negative stereotype was not primed, the self-esteem of the LD students was significantly influenced by the feedback of the task: an enhance self-esteem following a positive feedback and a lower self-esteem following a negative feedback. When the negative stereotype was primed, there was no significantly difference between the positive feedback group and negative feedback group. All the results showed that priming the negative stereotype could weaken the influence of feedback to the self-esteem of LD students. 5. There was more cognitive and behavioral control when LD students tried to cope with the stigma by concealing negative academic achievement during an individual interview with an unfamilar expert. The LD students whose academic achievements could be concealed had more thought suppression and thought intrusion and reported more self-monitoring behavior than the participants in the other experimental conditions.