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Consider one-dimensional flow through a confined porous aquifer of total thickness \(b\) and crosssectional area \(A\). Suppose the aquifer consists of \(N\) layers, each of thickness \(b_{i}(i=1, \ldots, N)\) and permeability \(k_{i}(i=1, \ldots, N) .\) Determine the total flow rate through the aquifer if all the layers are subjected to the same driving pressure gradient. What is the uniform permeability of an aquifer of thickness \(b\) that delivers the same flow rate as the layered aquifer when the two are subjected to the same pressure gradient?

Short Answer

Expert verified
Total flow rate is \(Q = -\frac{A (\nabla P)}{\mu} \sum_{i=1}^N (k_i b_i)\) and uniform permeability is \(k_e = \frac{1}{b} \sum_{i=1}^N (k_i b_i)\).

Step by step solution

01

Understand the Problem

We need to find the total flow rate through an aquifer composed of multiple layers, each with its own thickness and permeability. Additionally, we need to determine the equivalent uniform permeability of the entire aquifer.
02

Set Up the Known Parameters

Let the depth of the aquifer be \(b\), and it has \(N\) layers. Each layer \(i\) has thickness \(b_i\) and permeability \(k_i\). The cross-sectional area of the aquifer is \(A\). All layers are subjected to the same pressure gradient, \(abla P\).
03

Equation for Flow Rate through a Layer

The flow rate through a single layer \(i\) can be expressed using Darcy's law: \[Q_i = -\frac{k_i A (abla P)}{\mu} b_i \]where \(Q_i\) is the flow rate, \(\mu\) is the fluid's dynamic viscosity, and \(abla P\) is the pressure gradient.
04

Calculate Total Flow Rate

Since each layer provides a parallel pathway for flow, the total flow rate \(Q\) is the sum of flow rates across all layers:\[Q = \sum_{i=1}^N Q_i = -\frac{A (abla P)}{\mu} \sum_{i=1}^N (k_i b_i)\]
05

Find Equivalent Uniform Permeability

We want to find a uniform permeability \(k_e\) for the entire aquifer of thickness \(b\) that results in the same total flow rate. According to Darcy’s law for the entire aquifer, \[Q = -\frac{k_e A (abla P)}{\mu} b\]Equate the total flow rate equations from the layered and equivalent uniform permeability: \[k_e b = \sum_{i=1}^N (k_i b_i)\]So the equivalent permeability \(k_e\) is given by:\[k_e = \frac{1}{b} \sum_{i=1}^N (k_i b_i)\]
06

Verify the Equation Dimensions

Ensure that both sides of the equation for \(k_e\) have consistent dimensional units, indicating correct formulation. The unit verification for permeability equation helps confirm the calculations are dimensionally consistent.

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Key Concepts

These are the key concepts you need to understand to accurately answer the question.

Permeability
Permeability is a measure of how easily fluids can pass through a porous material. In the context of a confined aquifer, where you have multiple layers of sediments each with their own permeability, it becomes important to understand how permeability affects the movement of water through the aquifer.
Each layer in an aquifer has its unique permeability value, represented by the symbol \( k \). This parameter is crucial because it determines how much water can flow through the layer; higher permeability means the water moves more freely.
  • Permeability is generally measured in units like darcies or millidarcies.
  • It's directly proportional to the flow rate—higher permeability means a higher potential flow rate.
  • In aquifers, knowing the permeability of each layer helps in predicting how water will travel through the subsurface.
Understanding permeability is essential for managing water resources, especially in environmental engineering and hydrology.
Porous Media Flow
Porous media flow refers to the movement of fluid through materials that have lots of tiny holes or pores, like sedimentary rocks or soil. This concept is central when discussing aquifers, which consist of layers of porous material that allow water to flow through them.
In the exercise, we explore the flow through a confined aquifer, emphasizing how water moves through each layer of sediment. Darcy’s Law becomes instrumental here as it provides a mathematical framework to describe and quantify this flow based on the permeability and pressure gradient.
  • Porous media flow relies on the structure and connectedness of the pores, which influences how easily fluids can pass through.
  • This kind of flow is characterized by slow movement, yet it's essential to the natural water cycle as it contributes to groundwater recharge.
Understanding this concept helps in designing ways to efficiently manage water extraction from aquifers.
Pressure Gradient
The pressure gradient in an aquifer is the change in pressure per unit distance in a given direction. It's this gradient that drives the flow of fluids through the aquifer. In Darcy's Law, the pressure gradient is a primary force that determines the flow rate of groundwater through the porous media.
A uniform pressure gradient across the layers of a confined aquifer ensures that each layer contributes to the total flow rate. The gradient, often represented as \( abla P \), is crucial because:
  • It's the difference in pressure that encourages the movement of water from high to low-pressure areas.
  • The steeper the gradient, the faster the flow of fluid, assuming constant permeability.
In practice, knowing the pressure gradient helps predict how quickly water can be drawn from an aquifer and can impact pumping strategies for water supply.
Confined Aquifer
A confined aquifer is a type of aquifer that is sandwiched between two impermeable layers. These layers effectively trap water inside, creating pressure. This setup ensures that water within the confined aquifer is under greater pressure than the water table in unconfined aquifers, which leads to some unique flow characteristics.
In our exercise, the aquifer consists of multiple layers, each contributing to overall distribution and flow. Key points about confined aquifers include:
  • Water in confined aquifers is often under artesian pressure, meaning it can rise above the top of the aquifer layer when penetrated by a well.
  • These aquifers are less susceptible to contamination from surface activities due to their protective spoil layers.
Understanding these layers' dynamics is crucial for sustainable water extraction and aquifer management.
Hydraulic Conductivity
Hydraulic Conductivity is a vital property of porous media that measures how readily water can move through it. Similar to permeability, it incorporates both the medium's properties and the fluid's properties. It's an important parameter in groundwater studies for assessing how easily water can be extracted from an aquifer.
Given its role in Darcy's Law, hydraulic conductivity (often symbolized as \( K \)) is defined as a ratio involving both intrinsic permeability and the fluid's viscosity:
  • It is expressed in units of velocity, often meters per second (m/s).
  • A higher conductivity value indicates that water can flow more freely through the aquifer material.
  • It takes into account both the permeability of the aquifer and the properties of the fluid, such as temperature and viscosity.
This concept is key for calculating water movement in aquifers and plays a pivotal role in water resource management and engineering.

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Most popular questions from this chapter

To derive an upward flow in a porous medium, it is clear that pressure must increase more rapidly with depth \(y\) than it does when the fluid is motionless. Use this idea to justify writing Darcy's law for vertical flow in a porous medium in the form $$ v=-\frac{k}{\mu}\left(\frac{d p}{d y}-\rho g\right) $$ where \(v\) is the vertical Darcy velocity (positive in the direction of increasing depth), \(\rho\) is the fluid density, and \(g\) is the acceleration of gravity. Consider a porous medium lying on an impermeable surface inclined at an angle \(\theta\) to the horizontal. Show that Darcy's law for the downslope volumetric flow rate per unit area \(q\) is $$ q=-\frac{k}{\mu}\left(\frac{d p}{d s}-\rho g \sin \theta\right) $$ where \(s\) is the downslope distance and \(q\) is positive in the direction of \(s\).

Assume that a porous medium can be modeled as a cubic matrix with a dimension \(b\); the walls of each cube are channels of thickness \(\delta\). (a) Determine expressions for the porosity and permeability in terms of \(b\) and \(\delta .\) (b) What is the permeability if \(b=0.1 \mathrm{~m}\) and \(\delta=1 \mathrm{~mm} ?\)

Consider an unconsolidated (uncemented) layer of soil completely saturated with groundwater; the water table is coincident with the surface. Show that of d the upward Darcy velocity \(|v|\) required to fluidize the bed is $$ |v|=\frac{(1-\phi) k g\left(\rho_{s}-\rho_{w}\right)}{\mu} $$ where \(\phi\) is the porosity, \(\rho_{s}\) is the density of the soil particles, and \(\rho_{w}\) is the water density. The condition of a fluidized bed occurs when the pressure at depth in the soil is sufficient to completely support the weight of the overburden. If the pressure exceeds this critical value, the flow can lift the soil layer.

Calculate pressure as a function of depth in a vapor-dominated geothermal system consisting of a near-surface liquid layer \(400 \mathrm{~m}\) thick overlying a wet steam reservoir in which the pressure-controlling phase is vapor. Assume that the hydrostatic law is applicable and that the liquid layer is at the boiling temperature throughout. Assume also that the steam reservoir is isothermal.

Determine the minimum critical Rayleigh number for the onset of convection in a layer of porous material heated from below with an isothermal and impermeable lower boundary and an isothermal constant pressure upper boundary. This boundary condition corresponds to a permeable boundary between a saturated porous layer and an overlying fluid. What is the horizontal wavelength that corresponds to the minimum value of \(\mathrm{Ra}_{\mathrm{cr}}\) ? Take the layer thickness to be \(b\), and let the upper boundary, \(y=0\), have temperature \(T=T_{0}\) and the lower boundary, \(y=b\), have temperature \(T=T_{1}\). Assume that at the onset of convection \(T^{\prime}\) has the form $$ T^{\prime}=T_{0}^{\prime} \sin \frac{2 \pi x}{\lambda} Y(y) $$ and show that \(Y(y)\) is a solution of $$ \frac{d^{4} Y}{d \bar{y}^{-4}}-2 a^{2} \frac{d^{2} Y}{d y^{-2}}+Y\left(a^{4}-a^{2} R a\right)=0 $$ where $$ a \equiv \frac{2 \pi b}{\lambda} \quad \bar{y} \equiv \frac{y}{b} $$ Show that the general solution of Equation (9.135) can be written as $$ Y=c_{1} e^{\gamma \bar{y}}+c_{2} e^{-\gamma \bar{y}}+c_{3} \sin \delta \bar{y}+c_{4} \cos \delta \bar{y} $$ where \(c_{1}, c_{2}, c_{3},\) and \(c_{4}\) are constants of integration and $$ \begin{array}{l} \gamma^{2}=a^{2}+a \sqrt{\mathrm{Ra}} \\ \delta^{2}=a \sqrt{\mathrm{Ra}}-a^{2} \end{array} $$ Show that the boundary conditions are $$ \begin{aligned} Y=0 & \text { on } \bar{y}=0 \text { and } 1 \\ \frac{d^{2} Y}{d y^{2}}=0 & \text { on } \bar{y}=1 \\ \frac{d}{d \bar{y}}\left(\frac{d^{2} Y}{d \bar{y}^{2}}-a^{2} Y\right)=0 & \text { on } \bar{y}=0 . \end{aligned} $$ Substitute Equation (9.137) into each of these boundary conditions to obtain four homogeneous equations for the four unknown constants \(c_{1}, c_{2},\) \(c_{3},\) and \(c_{4} .\) Show that a nontrivial solution of these equations requires $$ \gamma \tan \delta+\delta \tanh \gamma=0 $$ This transcendental equation is an eigenvalue equation that implicitly gives \(\mathrm{Ra}_{\mathrm{cr}}\) as a function of \(a\), since both \(\gamma\) and \(\delta\) are defined in terms of \(\mathrm{Ra}\) and \(a\) in Equations (9.138) and (9.139) . The critical Rayleigh number can be found by numerically solving Equations (9.138),(9.139) , and (9.143) . The value of min \(\left(\mathrm{Ra}_{\mathrm{cr}}\right)\) turns out to be \(27.1 .\) One way of proceeding is to choose a value of \(a\) (there exists an \(\mathrm{Ra}_{\mathrm{cr}}\) for each a). Then try a value of \(\delta\). Compute \(\gamma\) from \(\gamma^{2}=2 a^{2}+\) \(\delta^{2} .\) Then compute \(\tan \delta / \delta\) and \(-\tanh \gamma / \gamma\). Iterate on \(\delta\) until these ratios are equal. With \(\delta\) determined \(\mathrm{Ra}_{\mathrm{cr}}\) follows from Equation \((9.139) .\) Repeat the process for different values of \(a\) until \(\min \left(\operatorname{Ra}_{c r}\right)\) is found.

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