【摘要】：本文利用有限差分?jǐn)?shù)值模擬技術(shù)研究了巖溶含水系統(tǒng)在有降雨入滲的情況下的演化過程,以及不同降雨量對(duì)巖溶含水系統(tǒng)發(fā)育的影響。在總結(jié)前人的研究成果的基礎(chǔ)上,構(gòu)建了巖溶含水系統(tǒng)概念模型,模型假設(shè)研究區(qū)的范圍為2200mⅹ800m的完整碳酸鹽巖體,模型左側(cè)、右側(cè)的垂直邊界及底部的水平邊界為隔水邊界,模型頂部為降雨入滲邊界,并且假設(shè)降雨入滲系數(shù)為0.3,模型中間的河谷地段為一地表水體,水頭為600m。為了使模型能夠更加直實(shí)可靠,利用Monte-Carle方法生成兩組隨機(jī)裂隙來代表實(shí)際巖體中的微小裂隙及各級(jí)結(jié)構(gòu)面,對(duì)于發(fā)育規(guī)模較大的斷層則直接輸入原始裂隙的坐標(biāo)及隙寬等參數(shù)。在對(duì)模型進(jìn)行數(shù)值計(jì)算時(shí),假定模型中的裂隙為二維光滑平行板裂隙,裂隙中的水流運(yùn)動(dòng)服從立方定律,并根據(jù)前人的實(shí)驗(yàn)成果,當(dāng)Re500時(shí)對(duì)立方定律進(jìn)行修正,然后利用裂隙網(wǎng)絡(luò)中的結(jié)點(diǎn)流量水均衡原理建立線性代數(shù)方程組,并用迭代法求解方程組。當(dāng)求出巖溶含水系統(tǒng)中裂隙網(wǎng)絡(luò)的各個(gè)結(jié)點(diǎn)水頭值后,假定在一個(gè)時(shí)間步長(zhǎng)內(nèi)巖溶含水系統(tǒng)中的裂隙網(wǎng)絡(luò)結(jié)點(diǎn)水頭穩(wěn)定,由此便可依據(jù)Palmer的實(shí)驗(yàn)得出的碳酸鹽巖溶蝕經(jīng)驗(yàn)公式求解巖溶含水系統(tǒng)的裂隙溶蝕速率,及經(jīng)過一定時(shí)間步長(zhǎng)溶蝕后的新的裂隙隙寬。求出新的裂隙隙寬后,便可重新進(jìn)行上一步的水頭計(jì)算,并依次計(jì)算每一個(gè)時(shí)間步長(zhǎng)內(nèi)的裂隙溶蝕溶率及裂隙發(fā)育情況。此外,還進(jìn)行了裂隙溶蝕的理論解計(jì)算與程序的數(shù)值解計(jì)算的對(duì)比,結(jié)果證明了程序的可靠性。本次研究模擬了巖溶含水系統(tǒng)由于裂隙發(fā)育的不均勻?qū)е碌牟町愋匀芪g現(xiàn)象,模型的模擬結(jié)果再現(xiàn)了巖溶含水系統(tǒng)自我演化過程中不同階段的演化特點(diǎn),并定量地給出了巖溶溶蝕過程中兩個(gè)出露于模型右邊界的巖溶泉的泉流量變化及模型中的含水介質(zhì)場(chǎng)的演變數(shù)據(jù)。在經(jīng)過10000年溶蝕后,泉1的流量由初始的0.45ml/s加大到6100年時(shí)的9e3ml/s,并在6100年后干涸,泉2的流量由初始的0.33ml/s加大到最后的2.6e5ml/s,裂隙的初始平均隙寬由0.1mm增大到10000年時(shí)的0.813mm。在模擬過程中發(fā)現(xiàn),巖溶含水系統(tǒng)的演化成熟度及演化速率與降雨量成正相關(guān),巖溶含水系統(tǒng)的溶蝕主要發(fā)生在潛水面附近及巖溶含水系統(tǒng)的源匯處,在深部巖溶并不發(fā)育,并且在同一范圍內(nèi)的不同組裂隙在巖溶含水系統(tǒng)的不同部位發(fā)育速率是不同的,這主要是由巖溶含水系統(tǒng)的介質(zhì)場(chǎng)演化是由水力梯度、大氣降雨量、巖石巖性等多方面因素共同決定的。
[Abstract]:In this paper, the evolution process of karst water-bearing system under the condition of rainfall infiltration and the influence of different rainfall on the development of karst water-bearing system are studied by using finite difference numerical simulation technique. On the basis of summarizing the previous research results, a conceptual model of karst water-bearing system is constructed. The model assumes that the range of the study area is 2200m x 800m complete carbonate rock mass, the left side of the model. The vertical boundary on the right side and the horizontal boundary at the bottom are water barrier boundaries, and the top of the model is the rainfall infiltration boundary. The rainfall infiltration coefficient is assumed to be 0.3, and the valley section in the middle of the model is a surface water body with a water head of 600 m. In order to make the model more direct and reliable, two groups of random fractures are generated by Monte-Carle method to represent the small fractures and their structural planes in real rock mass, and the parameters such as coordinate and gap width of the original fractures are directly input to the faults with large scale. In the numerical calculation of the model, the fracture in the model is assumed to be a two-dimensional smooth parallel plate fissure, and the flow motion suit in the fissure follows the cubic law. According to the previous experimental results, the opposite square law is modified when Re500 is used. Then the linear algebraic equations are established by using the equilibrium principle of nodal flow and water in the fracture network, and the equations are solved by iterative method. When the water head values of each node in the karst water-bearing system are calculated, it is assumed that the water head of the fissure network in the karst water-bearing system is stable in a time step. According to the empirical formula of carbonate rock dissolution obtained by Palmer's experiment, the dissolution rate of karst water bearing system and the new crack width after a certain time step dissolution can be solved. After the new crack gap width is obtained, the head calculation of the previous step can be carried out again, and the dissolution rate and fracture development of the fracture within each time step can be calculated in turn. In addition, the calculation of the theoretical solution of fracture dissolution is compared with that of the numerical solution of the program. The results show that the program is reliable. In this study, the different dissolution phenomena of karst water-bearing system caused by uneven fissure development are simulated. The simulation results of the model reproduce the evolution characteristics of karst water-bearing system in different stages in the process of self-evolution. The variation of spring discharge of two karst springs exposed to the right boundary of the model and the evolution data of the water-bearing medium field in the model are given quantitatively. After 10, 000 years of dissolution, the flow rate of Quan 1 increased from initial 0.45ml/s to 9e3ml / s at 6100, and dried up after 6100. The flow of Spring 2 increased from initial 0.33ml/s to last 2.6e5ml / s, and the initial average gap width of fissures increased from 0.1mm to 0.813mm. In the process of simulation, it is found that the evolution maturity and evolution rate of karst water-bearing system are positively related to rainfall. The dissolution of karst water-bearing system mainly occurs near the phreatic surface and the source and sink of karst water-bearing system, and does not develop in the deep karst. And the different groups of cracks in the same range have different developing rates in different parts of karst water-bearing system. This is mainly due to the evolution of the medium field of karst water-bearing system from hydraulic gradient and atmospheric rainfall. Rock lithology and other factors together determine.
【學(xué)位授予單位】：中國(guó)地質(zhì)大學(xué)(北京)
【學(xué)位級(jí)別】：碩士
【學(xué)位授予年份】：2015
【分類號(hào)】：P641.134

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