# GEO3020/4020 Lecture 1: Meteorological elements

## Presentation on theme: "GEO3020/4020 Lecture 1: Meteorological elements"— Presentation transcript:

GEO3020/4020 Lecture 1: Meteorological elements
Repetition

Weather is determined by the energy and mass transport at the surface:
Meteorological variables are used to describe the weather and to calculate the components of the energy and water balance equation.

Meteorological variables
Precipitation Radiation Air temperature Air humidity Wind Air pressure

Radiation Why do we want to calculate the radiation budget at the land surface?

70% 30%

Important contributor to the energy balance at the earth surface; Difficult to measure; Method for estimating it on a horisontal and slope surface at an arbritary place is given in Appendix E.

Summary = Extraterrestrial Radiation on a sloping plane
= Extraterrestrial Radiation on a horizontal plane = Extraterrestrial Radiation on a sloping plane = Total daily clear sky incident radiation on a horizontal plane at the earth surface = global short wave radiation at the earth surface = backscattered radiation (= ) and

The total daily clear sky radiation flux at the surface , are derived from Empirical relationships (adjusting for the effect of clouds and vegetation) have been developed, e.g. where global short wave radiation on the surface and , Extraterrestrial Radiation, n = actual sunshine hour and N= max sunshine hour (can be read from table for a given location and season).

Relation between K, Kin, Kcs, KET
KET = Extraterrestrial (potential) solar radiation Kcs = clear sky short wave radiation flux on a horizontal surface on earth Kin = adjusted Kcs for slope, aspect, clouds and vegetation K = net flux of solar energy entering the surface, e.g. snowpack Normally K < Kin < Kcs < KET KET = extraterrestrial (potential) solar radiation Kin = measured solar radiation

Structure of the atmosphere
Composition Vertical structure Pressure-temperature relation (Ideal gas law) Adiabatic lapse rate (dry & wet) Vapour Vapour pressure, ea Sat. vapour pressure, ea* Absolute humidity, ρv Specific humidity, q = ρa/ρv Relative humidity, Wa = ea/ea* Dew point temperature, Td The mass concentration of water vapour in a volume of air (vapour density) [kg m-3]

Meteorological variables Measurements
Precipitation Radiation Air temperature Air humidity Wind Air pressure Selve hytten er hvitmalt for å reflektere mest mulig solstråling, og skal plasseres i et åpent område, helst ikke i le av eller for nær bygninger og lignende hindringer som gir skygge. Underlaget under hytten skal være kortklipt gress. For eksempel kan asfalt ett sted og en fuktig myr et annet sted gi helt forskjellige målinger, særlig på varme, solrike sommerdager. Veggene i hytten er ikke helt tett, slik at det er godt ventilert og luften kan bevege seg fritt gjennom hytten. Termometeret er plassert inne i hytten, to meter over bakken. Inni hytten er termometeret beskyttet slik at solen ikke skinner direkte på det og varmer det opp, og det er også skjermet mot nedbør

GEO3020/4020 Lecture 2: I. Energy balance
Lena M. Tallaksen Chapter & 7.3.4, Appendix D.4; Dingman

70% 30%

Albedo is the shortwave reflectance

Net solar radiation, K K = Kin - Kout = Kin·(1-a) (5-27) Where K is net flux of solar energy entering the body Kin – flux of solar energy incident on the surface (= global radiation) Kout – reflected flux a – albedo, depends on the properties of the surface K can be measured by pyranometers, but more common to estimate Kcs represents the clear-sky shortwave radiation flux Kin, adjusted for the slope and aspect: Λ, latitude, J day of year, b, slope inclination angle, a, slope azimuth angle C, fraction of sky covered with clouds F, fraction of sky obscured by forest canopy, are functions

The function is derived using the concept of equivalent latitude, The function , the effect of cloud cover can be estimated using empirical relations like, or The function effect of forest canopy, an example for pine, The albedo, a, changes with location, season, vegetation, ….

Practical considerations
Empirical equation for Shortwave radiation C = fraction of sky covered with clouds KCS = total daily clear sky incident radiation on a horizontal plane at the earth surface

Net longwave radiation – equals to incoming atmospheric longwave radiation minus the portion of that reflected and the radiation flux emitted by the surface L = Lin – Lout = Lat – (1-es)Lat - Ls (7-28) where: Lat - incoming atmospheric longwave radiation flux, Ls - outgoing radiation from the surface es - emissivity of surface L, Lat, Ls can be measured by pyranometers, but more common to estimate using equations like: eat - emissivity of the atmosphere and canopy es - emissivity of the surface σ - Stefan-Boltzmann constant Tat ,Ts – temperature of the atmosphere and water surface

Combine the two equations (5.35 and 5.36) we get: where s, Stefan-Boltzmann constant (4.90×10-9 MJ m-2 day-1 K-4) Tat, effective radiating temp of atmosphere and canopy (˚C) Ts, temperature of surface (˚C) Table D-1 for es values, the question remains how to calculate eat.

Table d1

Clear sky, no forest canopy Cloudy sky, no forest canopy Cloudy sky, forest canopy (general equation) where ea is near surface saturation atmospheric vapor pressure and Ta is air temperature in °C, F is the ratio of the horizontally projected area of forest canopy to the total area of interest, C is degree of cloud cover

30% 70%

Sensible heat, H Sensible-heat exchange by turbulent transfer, H:
and from equation (D-49) where ra = density of air; Ca = heat capacity of air; k = 0.4; zd = zero plane displacement height z0 = surface-roughness height; za = height above ground surface at which va & Ta are measured; va = windspeed, Ta = air temperatures and Ts = surface temperatures.

Zveg Z0 Zd velocity

Latent heat, LE Latent heat exchange by turbulent transfer, LE
and from equation (D-42) where ra = density of air; λv = latent heat of vaporization; P = atmospheric pressure k = 0.4; zd = zero plane displacement height z0 = surface-roughness height; za = height above ground surface at which va & ea are measured; va = horisontal windspeed, ea = air vapor pressure es = surface vapor pressure (measured at z0 + zd)

Exchange of (sensible) heat with the ground, G
Positive or negative depending on the temperature of the air and soil surface (often negligible compared to other terms). If soil temperature is increasing downward (due to thermal energy stored during the summer) heat is transferred upwards at a rate: kG is the thermal conductivity of the soil (E L-1 T-1 q-1), depends on soil texture, soil density, and moisture content and vary widely with season and place.

Net water-advected energy Aw [E L-2 T-1] is found from: where: rw density of water [M L-3] cw – specific heat of water [E M-1 θ-1] w – average precipitation rate [L T-1] SW and GW – surface water and ground water inflows and outflows Ts – temperatures of the respective inflows and outflows [θ] Heat input by rain, R (snowpack) rainwater is first cooled to the snow temperature (Eq. 5-47a) if the snow is below zero, then freezing may occur and latent heat realised (Eq. 5-47b)

Change in stored energy, ΔQ
Energy can be stored in e.g. a snowpack, lake or soil Snow (warming phase) Lake where: hm snow water equivalent ci heat capacity of ice V lake volume, TL average lake temperature, AL lake area. subscripts 1 and 2 designate values at the beginning and end of Dt

Energy balance equation
where: K net shortwave radiation L net longwave radiation LE latent heat transfer H sensible heat transfer G soil flux Aw advective energy ΔQ/Δt change in stored energy Units: [EL-2T-1]

Calculation of evaporation using the energy balance method
Evaporation can be calculated solving for LE: where: LE has units [EL-2T-1] E [LT-1] = LE/ρwλv Latent Heat of Vaporization : lv= (2.361 × 10-3) Ta

Lena M. Tallaksen Chapter 7. – 7.1.2, 7.3.6; Dingman
GEO3020/4020 Lecture 2: II. Evapotranspiration - Definitions - Governing factors - Measurements Lena M. Tallaksen Chapter 7. – 7.1.2, 7.3.6; Dingman

Global water balance 765 114 1141 1255 490 275 mm/year

Water balance for Norway, 1931 -60

Evaporation - Norway

Global distribution of evaporation (cm)
Encyclopedia Britannica Inc.

Temporal variation – bare soil

Temporal variation – Lake Ontario

Evaporation and evapotranspiration
Summary Evapotranspiration is a collective term for all the processes by which water in the liquid or solid phase at or near the earth’s surface (rivers and lakes, bare soils, and vegetative surfaces) becomes atmospheric water vapor. Evapotranspiration is a second largest term in the global water balance; about 62% of precipitation that falls on the continents is evapotranspired. Evapotranspiration is the term that links earth surface’s water balance and energy balance. It is much more difficult to measure evapotranspiration than to measure precipitation and streamflow. There are numerous methods/models available in calculating evapotranspiration, of which the most well-known methods will be discussed in the class.

Governing factors of evaporation
I. Meteorological situation Energy availability How much water vapour can be received Temperature Vapour pressure deficit Wind speed and turbulence Optimal conditions: ?

Governing factors of evaporation
II. Physiographic and plant characteristics Characteristics that influence available energy albedo heat capacity How easily can water be evaporated size of the evaporating surface surroundings roughness (aerodynamic resistance) salt content stomata Water supply free water surface (lake, ponds or intercepted water) soil evaporation transpiration The wind speed immediately above the surface. The humidity gradient away from the surface. The rate and quantity of water vapor entering into the atmosphere both become higher in drier air. Water availability. Evapotranspiration cannot occur if water is not available.

Evapotranspiration Measurements
Free water evaporation Pans and tanks Evaporimeters Evapotranspiration (includes vegetation) Lysimeters Remote sensing

Definitions Potential evapotranspiration, PE, is the rate at which evapotranspiration would occur from a large area completely and uniformly covered with growing vegetation which has access to an unlimited supply of soil water and without advection or heat-storage effects (i.e. the rate is depedent on the vegetation) Actual evapotranspiration, ET, is the rate at which evapotranspiration occurs (i.e. describes all the processes by which liquid water at or near the land surface becomes atmospheric water vapor).

Pan evaporation methods
Epan = W – [V2-V1] where W = precipitation during Dt V1 = the storage at the beginning of Dt V2 = the storage at the end of Dt For American Class-A pan, Kohler et al. (1955) developed an empirical equation to account for energy exchange through sides of a pan, and adjust daily pan evaporation, Epan, to free water evaporation, Efw [mm day-1] (Equations 7-41 and 7-42).

Pan evaporation methods
Pan coefficient Elake/Epan = kp where k is a coefficient that varies with seasons and lake. Its annual average over the US is about 0.7

Pan evaporation methods

Pan evaporation methods
Example of pan coefficient in the Yangtze River catchment in China 46

Lysimeter One of the most reliable way of measuring potential or actual evapotranspiration is to use large containers (sometimes on the order of several metres across) called lysimeters; Evapotranspiration is calculated by subtraction considering the different components of the water balance. A lysimeter is most accurate when vegetation is grown in a large set up which allows the rainfall input and water lost through the soil to be easily calculated from the difference between the weight before and after a given period.

Lysimeter for measuring potential evapotranspiration
input (Rainfall R and Additional water A) and output (Percolated water P) collected in the receiver, then PE can be estimated from the equation: PE = R + A – P R A P

Lysimeter for measuring actual evapotranspiration
Figure. Schematic of a weighable gravitation lysimeter.

Estimation of evapotranspiration by remote sensing
Remote sensing has two potentially very important roles in estimating evapotranspiration (Engman, 1995). First, remotely sensed measurements offer methods for extending point measurements or empirical relationships to much larger areas, including those areas where measured meteorological data may be sparse. Secondly, remotely sensed measurements may be used to measure variables in the energy and moisture balance models of ET, such as as radiometric surface temperature, albedo, and vegetation index.