Subfield: Thermodynamics

CHANGE OF AIR TEMPERATURE WITH ALTITUDE, ATMOSPHERIC STABILITY AND AIR POLLUTION 

Vertical motion of air governs many atmospheric processes, such as the formation of clouds and precipitation and the dispersal of air pollutants. If the atmosphere is stable, vertical motion is restricted and air pollutants tend to be accumulated around the emission site rather than dispersed and diluted. Meanwhile, in an unstable atmosphere, vertical motion of air encourages the vertical dispersal of air pollutants. Therefore, the pollutants' concentrations depend not only on the strength of emission sources but also on the stability of the atmosphere.

We shall determine the atmospheric stability by using the concept of air parcel in meteorology and compare the temperature of the air parcel rising or sinking adiabatically in the atmosphere to that of the surrounding air. We will see that in many cases an air parcel containing air pollutants and rising from the ground will come to rest at a certain altitude, called a mixing height. The greater the mixing height, the lower the air pollutant concentration. We will evaluate the mixing height and the concentration of carbon monoxide emitted by motorbikes in the Hanoi metropolitan area for a morning rush hour scenario, in which the vertical mixing is restricted due to a temperature inversion (air temperature increases with altitude) at elevations above $119 \mathrm{~m}$.

Let us consider the air as an ideal diatomic gas, with molar mass $\mu=29 \mathrm{~g} / \mathrm{mol}$.

Quasi equilibrium adiabatic transformation obey the equation $p V^{\gamma}=$ const, where $\gamma=\frac{c_{p}}{c_{V}}$ is the ratio between isobaric and isochoric heat capacities of the gas.

The student may use the following data if necessary:

The universal gas constant is $R=8.31 \mathrm{~J} /($ mol.K).

The atmospheric pressure on ground is $p_{0}=101.3 \mathrm{kPa}$

The acceleration due to gravity is constant, $g=9.81 \mathrm{~m} / \mathrm{s}^{2}$

The molar isobaric heat capacity is $c_{p}=\frac{7}{2} R$ for air.

The molar isochoric heat capacity is $c_{V}=\frac{5}{2} R$ for air.



Mathematical hints 

a. $\int \frac{d x}{A+B x}=\frac{1}{B} \int \frac{d(A+B x)}{A+B x}=\frac{1}{B} \ln (A+B x)$

b. The solution of the differential equation $\frac{d x}{d t}+A x=B \quad$ (with $\quad A$ and $B$ constant) is $x(t)=x_{1}(t)+\frac{B}{A}$ where $x_{1}(t)$ is the solution of the differential equation $\frac{d x}{d t}+A x=0$.

c. $\lim _{x \rightarrow \infty}\left(1+\frac{1}{x}\right)^{x}=e$

1. Change of pressure with altitude.
Context question:
1.1. Assume that the temperature of the atmosphere is uniform and equal to $T_{0}$. Write down the expression giving the atmospheric pressure $p$ as a function of the altitude $z$.
Context answer:
\boxed{$p(z)=p(0) e^{-\frac{\mu g}{R T_{0}} z}$}


Extra Supplementary Reading Materials:

1.2. Assume that the temperature of the atmosphere varies with the altitude according to the relation

$$
T(z)=T(0)-\Lambda z
$$

where $\Lambda$ is a constant, called the temperature lapse rate of the atmosphere (the vertical gradient of temperature is $-\Lambda$ ).
Context question:
1.2.1. Write down the expression giving the atmospheric pressure $p$ as a function of the altitude $Z$.
Context answer:
\boxed{$p(z)=p(0)\left(1-\frac{\Lambda z}{T(0)}\right)^{\frac{\mu g}{R \Lambda}}$}


Context question:
1.2.2. A process called free convection occurs when the air density increases with altitude. At which values of $\Lambda$ does the free convection occur?
Context answer:
\boxed{$0.034$}


Extra Supplementary Reading Materials:

2. Change of the temperature of an air parcel in vertical motion

Consider an air parcel moving upward and downward in the atmosphere. An air parcel is a body of air of sufficient dimension, several meters across, to be treated as an independent thermodynamical entity, yet small enough for its temperature to be considered uniform. The vertical motion of an air parcel can be treated as a quasi adiabatic process, i.e. the exchange of heat with the surrounding air is negligible. If the air parcel rises in the atmosphere, it expands and cools. Conversely, if it moves downward, the increasing outside pressure will compress the air inside the parcel and its temperature will increase.

As the size of the parcel is not large, the atmospheric pressure at different points on



the parcel boundary can be considered to have the same value $p(z)$, with $z$ - the altitude of the parcel center. The temperature in the parcel is uniform and equals to $T_{\text {parcel }}(z)$, which is generally different from the temperature of the surrounding air $T(z)$. In parts 2.1 and 2.2, we do not make any assumption about the form of $T(z)$.
Context question:
2.1. The change of the parcel temperature $T_{\text {parcel }}$ with altitude is defined by $\frac{d T_{\text {parcel }}}{d z}=-G$. Derive the expression of $G\left(T, T_{\text {parcel }}\right)$.
Context answer:
\boxed{$\frac{\gamma-1}{\gamma} \frac{\mu g}{R} \frac{T_{\text {parcel }}}{T}$}


Extra Supplementary Reading Materials:

2.2. Consider a special atmospheric condition in which at any altitude $z$ the temperature $T$ of the atmosphere equals to that of the parcel $T_{\text {parcel }}, T(z)=T_{\text {parcel }}(z)$. We use $\Gamma$ to denote the value of $G$ when $T=T_{\text {parcel }}$, that is $\Gamma=-\frac{d T_{\text {parcel }}}{d z}$ (with $\left.T=T_{\text {parcel }}\right) . \Gamma$ is called dry adiabatic lapse rate.
Context question:
2.2.1. Derive the expression of $\Gamma$
Context answer:
\boxed{$\Gamma=\frac{\mu g}{c_{p}}$}


Context question:
2.2.2. Calculate the numerical value of $\Gamma$.
Context answer:
\boxed{$0.00978 $}


Context question:
2.2.3. Derive the expression of the atmospheric temperature $T(z)$ as a function of the altitude.
Context answer:
\boxed{$T(z)=T(0)-\Gamma z$}


Context question:
2.3. Assume that the atmospheric temperature depends on altitude according to the relation $T(z)=T(0)-\Lambda z$, where $\Lambda$ is a constant. Find the dependence of the parcel temperature $T_{\text {parcel }}(z)$ on altitude $z$.
Context answer:
\boxed{$T_{\text {parcel }}(z)=T_{\text {parcel }}(0)\left(\frac{T(0)-\Lambda z}{T(0)}\right)^{\frac{\Gamma}{\Lambda}}$}


Context question:
2.4. Write down the approximate expression of $T_{\text {parcel }}(z)$ when $|\Lambda z|<<T(0)$ and $T(0) \approx T_{\text {parcel }}(0)$.
Context answer:
\boxed{$T_{\text {parcel }}(0)-\Gamma z$}


Extra Supplementary Reading Materials:

3. The atmospheric stability. 

In this part, we assume that $T$ changes linearly with altitude.
Context question:
3.1. Consider an air parcel initially in equilibrium with its surrounding air at altitude



$z_{0}$, i.e. it has the same temperature $T\left(z_{0}\right)$ as that of the surrounding air. If the parcel is moved slightly up and down (e.g. by atmospheric turbulence), one of the three following cases may occur:

- The air parcel finds its way back to the original altitude $z_{0}$, the equilibrium of the parcel is stable. The atmosphere is said to be stable.
- The parcel keeps moving in the original direction, the equilibrium of the parcel is unstable. The atmosphere is unstable.
- The air parcel remains at its new position, the equilibrium of the parcel is indifferent. The atmosphere is said to be neutral.

What is the condition on $\Lambda$ for the atmosphere to be stable, unstable or neutral?
Context answer:
$\Lambda>\Gamma$ is unstable
$\Lambda<\Gamma$ is stable
$\Lambda=\Gamma$ is neutral


Context question:
3.2. A parcel has its temperature on ground $T_{\text {parcel }}(0)$ higher than the temperature $T(0)$ of the surrounding air. The buoyancy force will make the parcel rise. Derive the expression for the maximal altitude the parcel can reach in the case of a stable atmosphere in terms of $\Lambda$ and $\Gamma$.
Context answer:
\boxed{$h=\frac{1}{\Lambda}\left[T(0)-\left(\frac{(T(0))^{\Gamma}}{\left(T_{\text {parcel }}(0)\right)^{\Lambda}}\right)^{\frac{1}{\Gamma-\Lambda}}\right]$}


Extra Supplementary Reading Materials:

4. The mixing height 

Table 1 

Data recorded by a radio sounding balloon at 7:00 am on a November day in Hanoi.

| Altitude, m | Temperature, ${ }^{\circ} \mathrm{C}$ |
| :---: | :---: |
| 5 | 21.5 |
| 60 | 20.6 |
| 64 | 20.5 |
| 69 | 20.5 |
| 75 | 20.4 |
| 81 | 20.3 |
| 90 | 20.2 |
| 96 | 20.1 |
| 102 | 20.1 |
| 109 | 20.1 |
| 113 | 20.1 |
| 119 | 20.1 |
| 128 | 20.2 |
| 136 | 20.3 |
| 145 | 20.4 |
| 153 | 20.5 |
| 159 | 20.6 |
| 168 | 20.8 |
| 178 | 21.0 |
| 189 | 21.5 |
| 202 | 21.8 |
| 215 | 22.0 |
| 225 | 22.1 |
| 234 | 22.2 |
| 246 | 22.3 |
| 257 | 22.3 |
Context question:
4.1. Table 1 shows air temperatures recorded by a radio sounding balloon at 7:00 am on a November day in Hanoi. The change of temperature with altitude can be approximately described by the formula $T(z)=T(0)-\Lambda z$ with different lapse rates $\Lambda$ in the three layers $0<\mathrm{z}<96 \mathrm{~m}, 96 \mathrm{~m}<\mathrm{z}<119 \mathrm{~m}$ and $119 \mathrm{~m}<\mathrm{z}<215 \mathrm{~m}$.

Consider an air parcel with temperature $T_{\text {parcel }}(0)=22^{\circ} \mathrm{C}$ ascending from ground. On the basis of the data given in Table 1 and using the above linear approximation, calculate the temperature of the parcel at the altitudes of $96 \mathrm{~m}$ and $119 \mathrm{~m}$.
Context answer:
\boxed{$294.04$, $293.81 $}


Context question:
4.2. Determine the maximal elevation $H$ the parcel can reach, and the temperature $T_{\text {parcel }}(H)$ of the parcel.

$H$ is called the mixing height. Air pollutants emitted from ground can mix with the air in the atmosphere (e.g. by wind, turbulence and dispersion) and become diluted within this layer.
Context answer:
\boxed{142, 293.6}


Extra Supplementary Reading Materials:

5. Estimation of carbon monoxide (CO) pollution during a morning motorbike rush hour in Hanoi.
Hanoi metropolitan area can be approximated by a rectangle with base dimensions $L$ and $W$ as shown in the figure, with one side taken along the south-west bank of the Red River.



<img_4476>

It is estimated that during the morning rush hour, from 7:00 am to 8:00 am, there are $8 \times 10^{5}$ motorbikes on the road, each running on average $5 \mathrm{~km}$ and emitting $12 \mathrm{~g}$ of CO per kilometer. The amount of CO pollutant is approximately considered as emitted uniformly in time, at a constant rate $M$ during the rush hour. At the same time, the clean north-east wind blows perpendicularly to the Red River (i.e. perpendicularly to the sides $L$ of the rectangle) with velocity $u$, passes the city with the same velocity, and carries a part of the CO-polluted air out of the city atmosphere.

Also, we use the following rough approximate model:

- The CO spreads quickly throughout the entire volume of the mixing layer above the Hanoi metropolitan area, so that the concentration $C(t)$ of $\mathrm{CO}$ at time $t$ can be assumed to be constant throughout that rectangular box of dimensions $L, W$ and $H$.
- The upwind air entering the box is clean and no pollution is assumed to be lost from the box through the sides parallel to the wind.
- Before 7:00 am, the $\mathrm{CO}$ concentration in the atmosphere is negligible.
Context question:
5.1. Derive the differential equation determining the CO pollutant concentration $C(t)$ as a function of time.
Context answer:
\boxed{$\frac{d C}{d t}+\frac{u}{W} C(t)=\frac{M}{L W H}$}


Context question:
5.2. Write down the solution of that equation for $C(t)$.
Context answer:
\boxed{$C(t)=\frac{M}{L H u}\left[1-\exp \left(-\frac{u t}{W}\right)\right]$}


Question: 5.3. Calculate the numerical value of the concentration $C(t)$ at 8:00 a.m.

Given $L=15 \mathrm{~km}, W=8 \mathrm{~km}, u=1 \mathrm{~m} / \mathrm{s}$.

Solution:
Taking as origin of time the moment 7:00 am, then 8:00 am corresponds to $t=3600 \mathrm{~s}$. Putting the given data in (15), we obtain :

$$
C(3600 \mathrm{~s})=6.35 \times(1-0.64)=2.3 \mathrm{mg} / \mathrm{m}^{3}
$$

Final answer: $2.3 $ $\mathrm{mg} / \mathrm{m}^{3}$