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© University of Reading 2008
Atmospheric Science Fieldcourse
September 5 2009
MicrometeorologySurface Layer Dynamics and Surface Energy ExchangeJanet Barlow and Andrew Ross
2
Aims of exercise
Micrometeorology is concerned with:– Interaction of atmosphere with the surface– Turbulent mixing
• Exchanges of momentum, heat, moisture…traces gases, aerosol
– Radiative energy exchange at the surface• Solar (shortwave)• Infra-red (longwave)
3
• Boundary Layer– Lowest part of troposphere– Few 10s of metres to ~2km deep– Interacts directly with surface:
• Feels the effect of friction• Heated/cooled by surface
– Dynamics are dominated by turbulence– Exhibits large diurnal changes in many properties:
depth, temperature…
Measuring the boundary layer
4
Temperature Profile
tropopause
free troposphere
boundary layer
temperatureinversion
stratosphere
April 24 2004
5
Humidity Profile
tropopause
inversion
6
Sources of Turbulence• Friction: mechanical
generation of turbulence– Flow over rough surface /
obstacles– Small perturbations of the
flow act as obstacles to the surrounding flow
– Shear in the flow can result in instability & overturning
• Turbulence results in a wind speed profile that is close to logarithmic
z
Wind speed
7
• Convection: – heating of air near the
surface (or cooling of air aloft) increases (decreases) its density with respect to the air around it, so that it becomes buoyant.
8
Surface energy budget
• Radiative transfer at the Earth’s surface dominates the production or suppression of turbulence in low wind conditions
• The heating of the lower layers of the atmosphere is governed by– Heating of the surface itself– Transfer of heat from the surface to the air by four processes:
• Absorption and emission of “natural” EM radiation at the surface
• Thermal conduction of heat energy within ground• Turbulent transfer of heat energy within the atmosphere• Evaporation of water stored in the surface layer or
condensation of water vapour onto surface
9
Sensibleheat flux
GroundHeat flux
Shortwaveradiation
Longwaveradiation
Flux densities = rate of transfer of energy across a surface
Sn= S↓- S↑ = (1-α)S↓
Ln=L↓-L↑
G
LE H
Latentheat flux
Rn
Netradiation
10
Surface energy balance
• Considering a thin layer of soil at the surface:
Heat storage = What goes in - what goes out!
For an infinitely thin layer – no heat storage therefore
Rn-G=H+LE
Where Rn = Sn+Ln
11
Ultimate aim of SEE/SLD sessions
• There are 3 ways of determining H, the sensible heat flux
1. SEE
Measure Rn and G
Estimate LE from met measurements using Penman-Monteith equation
Residual is H (assuming infinitely thin layer)
2. T profile
Take a logarithmic T profile from the mast
Find friction velocity and friction temperature
3. Turbulent eddy measurements
Measure heat flux due to turbulent eddies using sonic anemometer data
**TuCH p TwCH p
12
Ultimate aim of SEE/SLD sessions
• There are 3 ways of determining H, the sensible heat flux
1. SEE
Measure Rn and G
Estimate LE from met measurements using Penman-Monteith equation
Residual is H (assuming infinitely thin layer)
2. T profile
Take a logarithmic T profile from the mast
Find friction velocity and friction temperature
3. Turbulent eddy measurements
Measure heat flux due to turbulent eddies using sonic anemometer data
**TuCH p TwCH p
13
SEE Activity
1. Real-time calculation of radiation budget (using portable mast)
Estimates of surface albedo, emissivity, response time
2. Components of the surface energy budget for a time period, and link to meteorology (uses Excel worksheets extensively)
3. Estimate H
14
InstrumentsPyranometer
• Measures the flux of solar radiation (W m-2)
• Two instruments mounted back to back – measurement of downwelling and upwelling radiation
15
Pyrgeometer
• Measures flux of infrared radiation (W m-2)
16
Weather station and ground heat flux
• Ground heat flux is also measured using a plate buried below the ground.
• Weather station data is used to estimate LE using the Penman-Monteith method.
• H can be estimated by balancing the budget!
17
Ultimate aim of SEE/SLD sessions
• There are 3 ways of determining H, the sensible heat flux
1. SEE
Measure Rn and G
Estimate LE from met measurements using Penman-Monteith equation
Residual is H (assuming infinitely thin layer)
2. T profile
Take a logarithmic T profile from the mast
Find friction velocity and friction temperature
3. Turbulent eddy measurements
Measure heat flux due to turbulent eddies using sonic anemometer data
**TuCH p TwCH p
18
SLD 1 - T profile method
• Calculate and analyse temperature and wind profiles from the mast data for two one hour periods (one stable and one unstable). Use these to calculate H
• A standard result: under neutral conditions, surface layer winds and temperatures have a logarithmic form.
• H can be estimated using the values of u* and T* **TuCH p
19
Instruments
15m Mast
• Air temperature and wind speed are measured at 6 levels on the mast
• Also have soil temperature just below surface.
20
Key parts of SLD1
• Check offset correction is applied
• Plot timeseries of quantities to find a stable and unstable period
• Plot logarithmic profiles of u and T to find u* and
T*
• Calculate H
21
Ultimate aim of SEE/SLD sessions
• There are 3 ways of determining H, the sensible heat flux
1. SEE
Measure Rn and G
Estimate LE from met measurements using Penman-Monteith equation
Residual is H (assuming infinitely thin layer)
2. T profile
Take a logarithmic T profile from the mast
Find friction velocity and friction temperature
3. Turbulent eddy measurements
Measure heat flux due to turbulent eddies using sonic anemometer data
TwCH p **TuCH p
22
• 3-D air motion is broken down into 3 velocity components (all in m s-1):u horizontal, along mean
wind direction, positive in direction of mean wind
v horizontal, perpendicular to u, positive to left of mean wind direction.
w vertical, positive upwards
u
v
w
23
Eddy averaging
• Any quantity can be divided into mean and fluctuating terms:
• To look at turbulent fluxes we are most concerned with the fluctuating terms e.g. w’
24
Eddy mixes some air down & some air up
(K)
Z (
m)
w’ +vew’ -ve
Warmer air is moved upcooler air is moved down
Heat flux
Z (
m)
0Wind speed (m s-1)
Faster moving air is moved down, slower air is moved up
Momentum flux
Turbulent fluxes result from the physical movement of parcels of air with different properties: temperature, humidity, gas concentration, momentum…
25
26
SLD 2 - Turbulent Eddy Measurements
• Use sonic anemometer data to calculate surface heat flux
Sonic Anemometer
• Measures 3D wind components at very short intervals.
TwCH p
27
28
Key parts of SLD2
• Calculate u’ and w’ series from 15 minute sonic measurements
• Calculate vertical momentum flux
• Calculate u* and H
• Compare with T profile measurements
29
Summary
• The SEE and SLD are linked exercises in which you will use different methods to explore the surface layer.
• The three experiments will all estimate the value of H, the turbulent transfer of heat energy from the surface to the lower layers of the atmosphere.
• You should assess the quality and reliability of the different techniques and what the changing value of H tells you about the meteorological situation.
30
u
w = 0
Sonic axes tilted off vertical
m
m
u
w1tan
um
wm
31
um
wm
wt
ut
cossin
sincos
mmt
mmt
wuw
wuu
32
• For example, the wind stress at the surface (the vertical flux of horizontal momentum) is
where is air density, and U the wind speed.
More strictly it is
where u is the wind component in the direction of the mean wind direction and v the component perpendicular to the mean wind.
'Uw
2122' vwuw
• The wind stress is often represented by the friction velocity
21
* u
33
The turbulent flux of some quantity ‘x’ is determined by averaging the vertical exchange of parcels of air with different values of ‘x’.
Flux of x = 1 (w′1x′1 + w′2x′2 + …w′Nx′N) N
= w′x′
where w′N = wN – w
and an overbar signifies averaging