We have defined three mean variables, ${\overline{\theta}}_{v}$ , $\overline{q}$ , and , $\overline{{V}_{}}$ , and three eddy flux terms associated with these mean values, ${\overline{w\text{'}\theta \text{'}}}_{v}$ , $\overline{w\text{'}q\text{'}}$ , and $\overline{u\text{'}w\text{'}}$ . Let’s examine their behavior as a function of height in the daytime boundary layer (see figure below).

#### Check Yourself

First, start with some general observations:

- All these height variations scale with the PBL height, whether it be 1 km or 3 km.
- Eddy fluxes move quantities from higher to lower values. If a mean quantity increases with height, then the eddy flux will be downward (negative); if a mean quantity decreases with height, then the eddy flux will be upward (positive).
- The entrainment zone is a layer of mixing between the boundary layer and the free troposphere.

*Before you read on, make sure that you believe these three concepts. *

### Virtual Potential Temperature, ${\overline{\theta}}_{v}$

The ${\overline{\theta}}_{v}$ profile is superadiabatic near the surface due to contact with the heated surface, neutral in the middle, and stable above. Eddies can rise from the surface to a height where ${\overline{\theta}}_{v}$ equals its surface value (assuming no cloud formation and condensation). The mixed layer will grow if surface heating or increased humidity by evaporation causes the surface ${\overline{\theta}}_{v}$ to increase, which means that air parcels can rise and be neutrally buoyant at greater ${\overline{\theta}}_{v}$ aloft and thus greater heights.

We see that the eddy flux ${\overline{w\text{'}\theta \text{'}}}_{v}$ is greatest at the surface, decreases nearly linearly with height, becomes slightly negative above the PBL height ${z}_{i}$ because eddies are bringing warmer air down from above so that ${\overline{w\text{'}\theta \text{'}}}_{v}<0$ . Remember, eddy fluxes carry z quantity like virtual potential temperature down the mean gradient.

### Specific Humidity, $\overline{q}$

Specific humidity originates at the surface, falls off slowly with height until it reaches the PBL height, and then falls off rapidly into the free atmosphere. Because $\overline{q}$ falls off with height, the humidity flux $\overline{w\text{'}q\text{'}}$ increases with height until $\overline{w\text{'}q\text{'}}$ becomes small because $\overline{q}$ becomes small.

### Horizontal Momentum Flux

$\overline{{V}_{}}$, the mean horizontal wind speed, increases logarithmically with height and then takes a jump above the PBL height as the wind no longer feels the friction from Earth’s surface and becomes geostrophic. The dashed line in the figure above indicates what the geostrophic wind would be without boundary layer friction. Because $\overline{{V}_{}}$is increasing with height, the horizontal momentum flux is negative throughout the boundary layer. It becomes less negative in the entrainment zone and approaches zero at heights above z_{i}.

So what does the daytime convective boundary layer look like? There are isolated convective updrafts surrounded by slower descending air, giving rise to the large-scale eddy circulation, as seen in the following video of the convective boundary layer, viewed from the top. Associated with the large eddies are smaller eddies that come about as the upward and downward air parcels move past each other. If you look closely, you will see eddies of all sizes in the video (:24), some quite large and some quite small, but the smaller ones seem to originate in the larger ones.

#### Quiz 11-2: State of flux.

- Find
**Practice Quiz 11-2**in Canvas. You may complete this practice quiz as many times as you want. It is not graded, but it allows you to check your level of preparedness before taking the graded quiz. - When you feel you are ready, take
**Quiz 11-2**. You will be allowed to take this quiz only**once**. Good luck!