# 1.3: Viscous Deformation

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Now we will cover the other type of deformation a rock can experience, viscous deformation. A simple model of viscous flow is seen below.** FIGURE viscous flow**. \(\Delta P=P_{pipe}-P_{o}\), where \(P_{o}\)=0. It is this pressure difference between the top and bottom of the pipe that drives the flow.

In geology, there are cases where viscous flow occurs, such as in river channels. Another example is in the **asthenosphere **(mantle). **FIGURE asthenosphere**. A final example is in a lava or glacial flow. **FIGURE Lava and Glacier**. How can we determine the flow of the previously mentioned cases? First, we need to derive some equations to better understand viscous flow.

**FIGURE force balance**

From the figure, we can see that A=\(\delta_{z} \cdot \delta_{y}\). We know from the last few sections that F=\(\sigma \cdot A\).

\[F=\sigma \cdot \delta_{z} \cdot \delta_{y}\]

Substituting in our equation for A, we get:

\[\frac{F}{\delta_z} =\sigma \cdot \delta_{y}\]

This is the force per unit length in 2D.

Now let's apply a velocity constraint.

**FIGURE velocity constraint**

\[\frac{d_{ux}}{d_y} \neq 0\]

This is the gradient in velocity

\[\frac{\frac{m}{s}}{m} = \frac{1}{s}\, ⇒ \text{strain rate}\]

\[\dot{\epsilon_s}=\frac{1}{2} \frac{d_{ux}}{d_y}\]

which is similar to

\[\epsilon=\frac{1}{2} \frac{\Delta x}{y}\]

From shear strain we can calculate shear stress.

\[\tau=2\mu\dot{\epsilon}=\mu\frac{d_u}{d_y}\]

**FIGURE shear stress**

All of the forces in the figure are acting in the x direction⇒ so they must balance.

\(F_s=\tau (y)(l)\)

\(\frac{d\tau}{dy}=\frac{dp}{dx}\), \(d\tau\) is in the x direction **FIGURE consv. momentum **

Let's now relate stress to flow.

\(\tau=\mu\frac{du}{dy}\)

\(\mu\frac{d^2 u}{dy^2}=\frac{dp}{dx}\) This is a differential equation, so now we will have to integrate with respect to y.

\(u=\frac{1}{2\mu} \frac{dp}{dx} y^2 +c_1 y+c_z\) This is the general form equation. You can see that there are several unknowns in the equation, the c's, that are a result of the integration. To solve for these, we must apply the equation to boundary value problems. We know that the conditions on boundaries lead to different solutions. There are two general types of flow that we will deal with, Couette Flow and flow down an inclined plane. We will examine Couette Flow first.

**FIGURE triangle u=0**

\(\frac{dp}{dx}\)=0 and \(u_o \neq 0\)

u(y=h)=0

u(y=0)=\(u_o\) (\(c_2 \Rightarrow u_o\))

\(\Rightarrow\) These are the boundary conditions we have been given for Couette Flow

Plugging in these boundry conditions gives us the solution: u=\(u_o (1-\frac{y}{h})\)

Using this, we can find the strain rate and stress.

\(\dot{\epsilon}=\frac{1}{2} \frac{du}{dy} =\frac{\mu_o}{2h}=\dot{\epsilon}\)

|\(\dot{\epsilon}| \sim \frac{\mu_o}{h}\)

Shear stress \(\sigma=2\mu\dot{\epsilon}\)=\(\mu\frac{du}{dy}=\frac{-\mu u_o}{h}\)

Now let's look into the asthenosphere and examine flow down an inclined plane.

**FIGURE asthenosphere**

u=\(u_o(1-\frac{u}{h})\)

From the figure, we are given that h \(\approx 100-150 km\) and \(v_p \approx 5 \frac{cm}{yr}\)

Using \(v_p\) and h, the strain rate is \(\dot{\epsilon}=\frac{1}{2} \frac{du}{dy}\) and the stress is \(\sigma=2\mu\dot{\epsilon}\)

Now let's look at the case of flow down an inclined plane. **FIGURE inclined plane**. Gravity, specifically \(g_x\), is the force driving the flow down the plane.

\(\sin(\alpha)=\frac{g_x}{g}\)

\(g_x=g\sin(\alpha)\)

We can also say that the pressure gradient drives the flow.

\(\Delta P=P_G-P_o-pg\sin(\alpha)\Delta x\), \(P_G\) and \(P_o\) are 0

\(\frac{\Delta P}{\Delta x}=-pg\sin(\alpha)\)

Finally, we get that \(\frac{dp}{dx}=-pg\sin(\alpha)\)

Substitute \(\frac{d\tau}{dy}=\frac{dp}{dx}\) into our previous general form equation,

\(u=\frac{1}{2\mu} (-pg\sin(\alpha))y^2 +c_1 y+c_2\). We still need our boundary conditions to solve the equation.

at y=h and u=0, \(c_1=\frac{pg\sin(\alpha)}{2\mu}h\)

at y=0 and u=\(c_2\), \(\tau=\mu\frac{du}{dy}=0\)

u=\(\frac{pg\sin(\alpha)}{2\mu}(h^2 -y^2)\) **FIGURE parabola/plate**

As we can see from the figure, \(u_{max} \Rightarrow y=0\)

Revising the strain rate equation, \(\dot{\epsilon}=\frac{1}{2} \frac{du}{dy}=\frac{pg\sin(\alpha)}{2y} y\)

**FIGURE parabola/plate pt 2** At \(\dot{\epsilon_max} \Rightarrow\) y=h

Thus, the strain rate (the rate at which strain is accumulating) ⇒ gradient in velocity, \(\neq\)velocity

It is important to note that the strain rate can be low even though the velocity is high.

Now let's look at some real world examples calculating strain rate. **FIGURE Lecture 4 strain rate**

The slope is \(\frac{\Delta e}{\Delta t}\)

=\(\frac{0.3}{1my}\cdot \frac{-1 my}{1e yr} \cdot \frac{1 yr}{3.15 e7 s}\)

=\(\frac{0.1}{1e13}=1e14 s^{-1}\) This is the strain rate

Strain rates are __very__ slow in the solid earth because rock deforms very slowly. But, other materials can deform much faster, such as an ice flow which deforms at about 1 inch a year. Flowing magma moves even faster, at about 1 inch per minute.

We are now going to cover one last concept related to viscous deformation, which is viscosity. Common viscous materials are honey and tar. Viscosity is represented by \(\eta\) and is time dependent.

\(\eta =\frac{\sigma}{2\dot{\epsilon}}\) and \(\eta\) has units of (Pa)(s).

For a solid rock, \(\eta \approx 10^{18} -10^{25}\) (Pa)(s) and

\(\dot{\epsilon} \approx 10^{-12} - 10^{-18} s^{-1}\)

Typical \(\dot{\epsilon}\) for the mantle is about \(10^{-15} s^{-1}\) and for a shear zone \(\dot{\epsilon}\) is about \(10^{-13} s^{-1}\).

Viscosity values for ice range from \(10^{11}-10^{13}\) (Pa)(s) and for lava \(10^{2}-10^{6}\) (Pa)(s).

The time scale for deformation is \(\tau \propto \frac{1}{\dot{\epsilon}} \cdot \frac{1s}{10^{-15}}\backsim \frac{10^{15}s\cdot yr}{3.15e7s} \cdot \frac{my}{1e6 yr} \approx 30 my\)

\(\tau \propto \frac{1}{10^{-18}} \Rightarrow 30 \cdot 1000 myr \Rightarrow 30Byr\) This is older than the age of the Earth, thus this is not deforming viscously.

Viscosity depends on a lot of properties of the rock and the physical conditions. Such properties include: composition, grain-size, water in minerals, presence of melt, presence of gar, and grains in the melt.