Karstification of aquifers interspersed with non-soluble rocks: From basic principles towards case studies
Karstification of aquifers interspersed with non-soluble rocks: From basic principles towards case studies
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散布着不溶性岩石的含水层岩溶作用：从基本原理到案例研究
DOI：
10.1016/j.enggeo.2010.09.008
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发表时间：
--
影响因子：
7.4
通讯作者：
Hiller
中科院分区：
文献类型：
--
作者：
Romanov;Kaufmann;Hiller
我们已经开发了一个数值模型，能够描述含水层的岩溶作用，在含有可溶性（石灰石或石膏）和不溶性层的断裂岩石。当水沿着穿过可溶层的裂缝流动时，它能够溶解那里的材料，以增加管道的孔径宽度，并因此增加局部水力传导性。取决于这些层的厚度和分布，溶解可以仅在有限的时间内或在整个演化时间内是活跃的。位于不溶性层中的裂缝根本不会改变。我们感兴趣的是这些当地的过程的整体效果，并研究四个简化的情况下，岩溶沿着一个突出的宽管道穿越破碎的石灰岩块。我们保持初始和边界条件相同的所有情况下，不同的只是可溶性物质的数量和分布。我们证明，含水层在100%的石灰岩，没有任何不溶层，发展沿着地区具有高水力传导率和高水力梯度，创造通道一样的途径。另一方面，含有厚度有限的可溶层的含水层发展较快，并呈现出由岩石的化学性质决定的扩散模式。论文的第二部分是对真实的岩溶系统建模的一个步骤。我们提出了位于附近的大型水工建筑物的含水层的演变。所有的初始和边界条件，除了可溶岩石的数量和分布，保持不变的所有方案。作为基岩的材料示例，我们选择了瑞士比尔斯河（Birs River）沿着含水层中的Gipskeuper。这种岩石由可溶性石膏层和不溶性粘土和泥灰岩组成，典型的层厚范围为毫米至厘米。本文第一部分讨论的基本过程仍然有效。我们表明，大的不溶区可以削弱岩溶作用过程，甚至完全阻止它，而薄的可溶层的区域可以提供一个优先的途径，大大减少了演化时间。最后，我们表明，含水层内的渗漏率和水头分布的演变，有时可以揭示有关岩溶作用的阶段和大坝的安全性误导信息。我们的模型不仅可以用来研究简化的地质环境和基本过程，而且还可以解决一些复杂的建模时产生的真实的含水层。
We have developed a numerical model able to describe the karstification of aquifers in fractured rocks containing soluble (limestone or gypsum) and insoluble layers. When water is flowing along fractures crossing the soluble layers, it is able to dissolve the material there, to increase the aperture width of the conduit, and consequently to increase the local hydraulic conductivity. Depending on the thickness and the distribution of these layers, the dissolution can be active only for limited periods, or during the whole evolution time. Fractures located in insoluble layers do not change at all. We are interested in the integral effect of these local processes and study four simplified scenarios of karstification along a prominent wide conduit crossing a fractured limestone block. We keep the initial and the boundary conditions the same for all scenarios and vary only in the amount and the distribution of the soluble material. We demonstrate that aquifers in 100% limestone, without any insoluble layers, develop along areas with high hydraulic conductivities and high hydraulic gradients, creating channel like pathways. On the other hand aquifers containing soluble layers with limited thickness develop faster and exhibit diffuse patterns determined by the chemical properties of the rock. The second part of the paper is a step towards modeling of real karst systems. We present the evolution of an aquifer located in the vicinity of a large hydraulic structure. All initial and boundary conditions, except the amount and the distribution of the soluble rock, remain the same for all scenarios. As a material example for the bedrock, we chose Gipskeuper from an aquifer along the Birs river in Switzerland. This rock consists of soluble gypsum layers and insoluble clays and marls, with typical layer thickness in the range of millimeters to centimeters. The basic processes discussed in the first part of the paper remain valid. We demonstrate that large insoluble zones can impair the karstification process and even completely block it, while areas with thin soluble layers can provide a preferential pathway and decrease the evolution times considerably. Finally we show that the evolution of the leakage rates and the head distribution within the aquifer can sometimes reveal misleading information about the stage of karstification and the safeness of the dam. Our model can be used not only to study simplified geological settings and basic processes, but also to address some of the complications arising when modeling real aquifers.
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