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If fluid is injected along a plane at \(x=0\) at a rate of \(0.1 \mathrm{~m}^{2} \mathrm{~s}^{-1}\), how high is the phreatic surface at the point of injection and how far has the fluid migrated if \(\mu=10^{-3} \mathrm{~Pa} \mathrm{~s}, \phi=0.1, k=10^{-11} \mathrm{~m}^{2}\) \(\rho=1000 \mathrm{~kg} \mathrm{~m}^{-3},\) and \(t=10^{5} \mathrm{~s}\) ? A MATLAB solu- tion to this problem is provided in Appendix \(D\).

Short Answer

Expert verified
Phreatic surface height is 1020.39 m; the fluid migrates approximately 0.354 m.

Step by step solution

01

Define the Known Variables

We start by listing the parameters given in the problem:- Injection rate (\(q_0 = 0.1 \text{ m}^2/\text{s}\)- Dynamic viscosity (\(\mu = 10^{-3} \text{ Pa} \cdot \text{s}\)- Porosity (\(\phi = 0.1\)- Permeability (\(k = 10^{-11} \text{ m}^2\)- Density (\(\rho = 1000 \text{ kg/m}^3\)- Time (\(t = 10^5 \text{ s}\)We are tasked to find the height of the phreatic surface at the point of injection and the distance the fluid has migrated.
02

Calculate Hydraulic Conductivity

The hydraulic conductivity (\(K\)) can be calculated using the formula: \[ K = \frac{k \cdot \rho \cdot g}{\mu} \]where \(g = 9.81 \text{ m/s}^2\) is the acceleration due to gravity.Substitute the known values:\[ K = \frac{10^{-11} \cdot 1000 \cdot 9.81}{10^{-3}} = 9.81 \cdot 10^{-8} \text{ m/s} \]
03

Determine the Height of the Phreatic Surface

The height \(h\) of the phreatic surface can be found using the equation:\[ h = \frac{q_0}{K \cdot W} \]where \(W\) is the width of the plane. Since \(W\) is not provided, it cancels out during consideration of symmetry.Thus:\[ h = \frac{0.1}{9.81 \times 10^{-8}} = 1020.39 \text{ m} \]
04

Calculate the Distance of Fluid Migration

The distance \(x\) of fluid migration is given by\[ x = 2 \times \sqrt{\frac{K \cdot \phi \cdot t}{\pi}} \]Substitute in the known values:\[ x = 2 \times \sqrt{\frac{9.81 \times 10^{-8} \cdot 0.1 \cdot 10^5}{\pi}} \]Calculate:\[ x \approx 2 \times 0.177 \approx 0.354 \text{ m} \]

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Key Concepts

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

Hydraulic Conductivity
Hydraulic conductivity (K) measures how easily water can move through pore spaces or fractures in a given material. It's similar to how efficiently electricity can pass through a wire, based on the wire's material properties. Hydraulic conductivity is an important factor in fluid dynamics, particularly in the context of groundwater flow.

The formula for hydraulic conductivity is given by:
  • K = \( \frac{k \cdot \rho \cdot g}{\mu} \),
where:
  • k is the permeability of the material,
  • \( \rho \) is the density of the fluid,
  • g is the acceleration due to gravity (approximately 9.81 m/se²), and
  • \( \mu \) is the dynamic viscosity of the fluid.
This relationship means that high hydraulic conductivity allows water to flow more easily, much like an open path through a sponge.
Phreatic Surface
The phreatic surface is essentially the boundary between the saturated and unsaturated zones in the ground. Think of it as the 'water table.' Above this level, the pore spaces in the substrate contain both air and water, while below it, they are completely filled with water.

When fluid is injected into the ground, it displaces the water table, causing it to rise or fall depending on the conditions. The height of the phreatic surface can be critical in managing groundwater resources, irrigation, and in the planning of structures that must be built on or near saturated soils. Typically, the height can be determined by considering the volume of fluid introduced relative to the material's properties like hydraulic conductivity and porosity.
Permeability
Permeability refers to the ability of a material to allow fluids to pass through it. Imagine trying to force water through a sieve — if the holes are large, water flows easily, indicating high permeability. Conversely, a fine mesh would slow down or stop the water flow, showing low permeability.

Permeability is a key parameter in the equation for hydraulic conductivity and is represented by "k" in the equation:
  • K = \( \frac{k \cdot \rho \cdot g}{\mu} \).
The unit of permeability is typically in square meters (m²). High permeability means that fluids can move freely through the material, which is crucial for tasks such as groundwater flow modeling and oil extraction.
Dynamic Viscosity
Dynamic viscosity (\( \mu \)) is the measure of a fluid's resistance to flow. This concept can be visualized by comparing honey, which flows slowly, to water, which flows quickly. Honey has a higher dynamic viscosity than water.

In fluid dynamics, dynamic viscosity influences how easily fluid moves through materials. It is an important part of calculating hydraulic conductivity. The lower the dynamic viscosity, the easier the fluid flows, much like a lubricated engine reduces resistance. The standard unit for dynamic viscosity is the Pascal-second (Pa⋅s).

In calculations, dynamic viscosity helps explain the relationship between the fluid's resistance against the surface it passes through, affecting everything from simple plumbing to complex groundwater flow systems.

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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 \(s\).

Consider a porous layer saturated with water that is at the boiling temperature at all depths. Show that the temperature-depth profile is given by $$ \frac{1}{T_{b 0}}-\frac{1}{T}=\frac{R_{v}}{L} \ln \left(1+\frac{\rho_{l} g y}{p_{0}}\right) $$ where \(T_{b 0}\) is the boiling temperature of water at atmospheric pressure \(p_{0}, \rho_{l}\) is the density of liquid water which is assumed constant, and \(R_{r}\) is the gas constant for water vapor. Start with the hydrostatic equation for the pressure and derive an equation for \(d T / d y\) by using the formula for the slope of the Clapeyron curve between water and steam $$ \frac{d p}{d T}=\frac{L \rho_{l} \rho_{v}}{T\left(\rho_{l}-\rho_{v}\right)} \approx \frac{L \rho_{v}}{T} $$ where \(\rho_{v}\) is the density of water vapor. Assume that steam is a perfect gas so that $$ \rho_{v}=\frac{p}{R_{r} T} $$ Finally, note that \(p=p_{0}+\rho_{l} g y\) if \(\rho_{l}\) is assumed constant. What is the temperature at a depth of \(1 \mathrm{~km}\) ? Take \(R_{v}=0.462 \mathrm{~kJ} \mathrm{~kg}^{-1} \mathrm{~K}^{-1}, L=2500 \mathrm{~kJ} \mathrm{~kg}^{-1}\) $$ T_{b 0}=373 \quad \mathrm{~K}, \quad p_{0}=10^{5} \quad \mathrm{~Pa}, \quad \rho_{l}=1000 \mathrm{~kg} \mathrm{~m}^{-3} $$ \(g=10 \mathrm{~m} \mathrm{~s}^{-2}\).

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.

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.

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.

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