Lincoln Zotarelli, Michael D. Dukes, Consuelo C. Romero, Kati W. Migliaccio, and Kelly T. Morgan^{2}
The term evapotranspiration (ET) is commonly used to describe two processes of water loss from land surface to atmosphere, evaporation and transpiration. Evaporation is the process where liquid water is converted to water vapor (vaporization) and removed from sources such as the soil surface, wet vegetation, pavement, water bodies, etc. Transpiration consists of the vaporization of liquid water within a plant and subsequent loss of water as vapor through leaf stomata.
Evaporation and transpiration occur simultaneously and both processes depend on solar radiation, air temperature, relative humidity (i.e., vapor pressure deficit) and wind speed. Transpiration rate is also influenced by crop characteristics, environmental aspects, and cultivation practices. Different kinds of plants may have different transpiration rates. Not only the type of crop, but also the crop development, environment, and management should be considered when assessing transpiration. For example, when the crop is small, water is predominately lost by soil evaporation because little of the soil surface is covered by the plant, but once the crop is well developed and completely covers the soil, transpiration becomes the main process (Allen et al. 1998).
Reference evapotranspiration (ET_{o}) is defined as the rate at which readily available soil water is vaporized from specified vegetated surfaces (Jensen et al. 1990). Then reference evapotranspiration is defined as the ET rate from a uniform surface of dense, actively growing vegetation having specified height and surface resistance, not short of soil water, and representing an expanse of at least 100 m of the same or similar vegetations (Allen et al. 2005). The concept of the ET_{o} was introduced to study the evaporative demand of the atmosphere independent of crop type, crop development, and management practices. If water is abundantly available at the reference surface, soil factors do not affect ET; however, ET may decrease overtime as soil water content decreases. Relating ET to a specific surface provides a reference to which ET from other surfaces can be related. It obviates the need to define a separate ET level for each crop and stage of growth and is referred to as crop ET (ET_{c}). ET_{o} values measured or calculated at different locations or in different seasons are comparable as they refer to the ET from the same reference surface. The only factors affecting ET_{o} are climatic parameters, and ET_{c} can be determined from ET_{o} using a crop specific coefficient (K_{c}). The use of K_{c} with specific crops is the subject of other EDIS documents: Basic Irrigation Scheduling in Florida (AE111; Smajstrla et al. 1997), Outline for Managing Irrigation of Florida Citrus with High Salinity Water (AE217; Boman and Stover 2002),
A WebBased Irrigation Scheduling Model to Improve Water Use Efficiency and Reduce Nutrient leaching for Florida Citrus (SS499; Morgan et al. 2009), Irrigation Scheduling for Tropical Fruit Groves in South Florida (AE21; Migliaccio and Li 2000), Smart Irrigation controllers: Programming Guidelines for EvapotranspirationBased Irrigation Controllers (AE445; Dukes et al. 2009) and Principle and Practices of Irrigation Management for Vegetables (Simonne et al. 2010).
A large number of empirical methods have been developed over the last 50 years to estimate evapotranspiration from different climatic variables. Some of these derived from the now wellknown Penman equation (Penman 1948) to determine evaporation from open water, bare soil, and grass (now called evapotranspiration) based on a combination of an energy balance and an aerodynamic formula, given as:
where λE= evaporative latent heat flux (MJ m^{2 }d^{1}), Δ= slope of the saturated vapor pressure curve [
e^{o}/
T, where e^{o} = saturated vapor pressure (kPa) and T_{mean} = daily mean temperature (°C)]; R_{n} = net radiation flux (MJ m^{2} d^{1}), G = sensible heat flux into the soil (MJ m^{2}d^{1}), ³ = psychrometric constant (kPa °C^{1}), and E_{a} = vapor transport of flux (mm d^{1}).
Various derivation of the Penman equation included a bulk surface resistance term (Monteith 1965), and the resulting equation is now called the PenmanMonteith equation, which may be expressed for daily values as:
where ρ_{a} = air density (kg m^{3}), C_{p} = specific heat of dry air, e_{s}^{o} = mean saturated vapor pressure (kPa) computed as the mean e^{o} at the daily minimum and maximum air temperature (°C), r_{av} = bulk surface aerodynamic resistance for water vapor (s m^{1}), e_{a} = mean daily ambient vapor pressure (kPa), and r_{s} = the canopy surface resistance (s m^{1}).
An updated equation was recommended by FAO (Allen et al. 1998) with the FAO56 PenmanMonteith Equation, simplifying equation 2 by utilizing some assumed constant parameters for a clipped grass reference crop. It was assumed that the definition for the reference crop was a hypothetical reference crop with crop height of 0.12 m, a fixed surface resistance of 70 s m^{1 }and an albedo value (i.e., portion of light reflected by the leaf surface) of 0.23 (Smith et al. 1992). The new equation is:
where ET_{o} = reference evapotranspiration rate (mm d^{1}), T = mean air temperature (°C), and u_{2} = wind speed (m s^{1}) at 2 m above the ground. Equation 3 can be applied using hourly data if the constant value "900" is divided by 24 for the hours in a day and the R_{n} and G terms are expressed as MJ m^{2 }h^{1}.
In 1999, the Irrigation Association (IA) requested the Evapotranspiration in Irrigation and Hydrology Committee – Environmental and Water Resources Institute (American Society of Civil Engineering)(ASCEET) to establish one standardized equation for estimating the parameters to gain consistency and wider acceptance of ET models (Howell and Evett 2006). The principal outcome was that two equations, one for a short crop (similar to clipped, coolseason grass) named ET_{os }and another for a tall crop (similar to fullcover alfalfa) named ET_{rs}, were developed for daily (24 hr) and hourly time periods. The ASCEEWRI standardized reference ET equation based on the FAO 56 PenmanMonteith equation (4) for a hypothetical crop is given as,
where ET_{sz} = the standardized reference evapotranspiration for grass (ET_{os}) or alfalfa (ET_{rs}) in units based on the time step of mm d^{1} for a 24h day or mm h^{1} for an hourly time step, C_{n} = the numerator constant for the reference crop type and time step and C_{d} = the denominator constant for the reference crop type and time step (see Table 1 for values of C_{n} and C_{d})
Note that ET_{sz} for a short crop (ET_{os}) equation is identical to the FAO56 PenmanMonteith equation previously described [Eq. 3]. The FAO56 equation has been selected because it closely approximates grass ET_{o} at the location evaluated, is physically based, and explicitly incorporates both physiological and aerodynamic parameters. FAO56 PenmanMonteith equation has been widely use for Florida conditions. Moreover, procedures have been developed for estimating missing climatic parameters (Allen et al. 2005; Romero et al. 2009).
The objective of this publication is to provide a stepbystep calculation of the reference evapotranspiration (FAO56 method) for a given location from the available weather data.
The reference evapotranspiration estimation method is based on climatic data, which can be obtained from a local weather station or, for Florida, can be obtained accessing the Florida Automated Weather Network (FAWN, http://fawn.ifas.ufl.edu/). The equation uses standard climatological records of solar radiation (sunshine), air temperature, humidity and wind speed. To ensure the integrity of computations, the weather measurements should be made at 2 m (or converted to that height) above an extensive surface of green grass, shading the ground and not short of water. Table 2 shows a list of parameters required to calculate ET_{o}.
The FAO PenmanMonteith method to estimate ET_{o} can be derived [Eq. 1]:
Where,
ET_{o} = reference evapotranspiration, mm day^{1};
R_{n} = net radiation at the crop surface, MJ m^{2} d^{1};
G = soil heat flux density, MJ m^{2} d^{1};
T = mean daily air temperature at 2 m height, °C;
u_{2} = wind speed at 2 m height, m s^{1};
e_{s} = saturation vapor pressure, kPa;
e_{a} = actual vapor pressure, kPa;
e_{s}e_{a} = saturation vapor pressure deficit, kPa;
Δ = slope of the vapor pressure curve, kPa ºC^{1};
γ= psychrometric constant, kPa °C^{1}.
The reference evapotranspiration, ET_{o}, provides a standard to which:
evapotranspiration at different periods of the year or in other regions can be compared;
evapotranspiration of other crops can be related.
Step 1: Mean daily temperature
The (average) daily maximum and minimum air temperatures in degrees Celsius (°C) are required. Where only (average) mean daily temperatures are available, the calculations can still be executed but some underestimation of ET_{o} will probably occur due to the nonlinearity of the saturation vapor pressure  temperature relationship (Allen et al. 1998). Average temperature is calculated by:
Where,
T_{mean} = mean daily air temperature, °C;
T_{max} = maximum daily air temperature, °C;
T_{min} = minimum daily air temperature, °C
Step 2: Mean daily solar radiation (R_{s})
The average daily net radiation expressed in megajoules per square meter per day (MJ m^{2} day^{1}) is required. A simple average of solar radiation values obtained from a weather station in the period of 24h (0:00:01 am to 11:59:59 pm) is required. The conversion of units may be required when solar radiation is expressed in watts per square meter per day (W m^{2} day^{1}).
Rs _{(MJ m}2_{day}1_{)} = R_{s (W m}2_{day}1_{)} * 0.0864 (Equation 6)
Step 3: Wind speed (u_{2})
The average daily wind speed in meters per second (m s^{1}) measured at 2 m above the ground level is required. It is important to verify the height at which wind speed is measured, as wind speeds measured at different heights above the soil surface differ. The wind speed measured at heights other than 2 m can be adjusted according to the follow equation:
Where, u_{2} = wind speed 2 m above the ground surface, m s^{1};
u_{z} = measured wind speed 2 m above the ground surface, m s^{1};
h = height of the measurement above the ground surface, m.
In case of wind speed is given in miles per hour (mi h^{1}) the conversion to m s^{1} is required.
u_{2 (m s}^{1}_{)} = u_{2} (mi h^{1}) (Equation 8)
Step 4: Slope of saturation vapor pressure curve (Δ)
For the calculation of evapotranspiration, the slope of the relationship between saturation vapor pressure and temperature, Δ, is required.
T_{mean} = mean daily air temperature, ºC, [Eq. 5]
exp = 2.7183 (base of natural logarithm).
Step 5: Atmospheric Pressure (P)
The atmospheric pressure, P, is the pressure exerted by the weight of the earth's atmosphere. Evaporation at high altitudes is promoted due to low atmospheric pressure. This effect is, however, small and in the calculation procedures, the average value for a location is sufficient. A simplification of the ideal gas law, assuming 20°C for a standard atmosphere, can be employed to calculate P in kPa at a particular elevation:
Where,
z = elevation above sea level, m.
Step 6: Psychrometric constant (γ)
The psychrometric constant relates the partial pressure of water in air to the air temperature so that vapor pressure can be estimated using paired dry and wet thermometer bulb temperature readings. Another way to describe the psychrometric constant is the ratio of specific heat of moist air at constant pressure (C_{p}) to latent heat of vaporization. The specific heat at constant pressure is the amount of energy required to increase the temperature of a unit mass of air by one degree at constant pressure. Its value depends on the composition of the air, i.e., on its humidity. For average atmospheric conditions a C_{p} value of 1.013 10^{3} MJ kg^{1} °C^{1} can be used. As an average atmospheric pressure is used for each location, the psychrometric constant is kept constant for each location depending of the altitude [Eq. 10].
γ = psychrometric constant, kPa °C1;
P = atmospheric pressure, kPa, [Eq. 10];
λ = latent heat of vaporization, 2.45, MJ kg^{1};
c_{p} = specific heat at constant pressure, 1.013 10^{3}, MJ kg^{1} °C^{1};
μ = ratio molecular weight of water vapour/dry air = 0.622.
Step 7: Delta Term (DT) (auxiliary calculation for Radiation Term)
In order to simplify the ET_{o} calculation, several terms are calculated separated. The delta term is used to calculate the Radiation Term of the overall ET_{o} equation (Eq. 33)
Where,
Δ = slope of saturation vapor curve [Eq.9];
γ = psychrometric constant, kPa °C^{1}, [Eq.11];
u_{2} = wind speed 2 m above the ground surface, m s^{1}, [Eq.7].
Step 8: Psi Term (PT) (auxiliary calculation for Wind Term)
The psi term is used to calculate the Wind Term of the overall ET_{o} equation [Eq. 34]
Where,
Δ = slope of saturation vapor curve [Eq. 9];
γ = psychrometric constant, kPa °C^{1}, [Eq. 11];
u_{2} = wind speed 2 m above the ground surface, m s^{1}, [Eq. 9].
Step 9: Temperature Term (TT) (auxiliary calculation for Wind Term)
The temperature term is used to calculate the Wind Term of the overall ET_{o} equation (Eq. 34)
Where,
T_{mean} = mean daily air temperature, ºC, [Eq. 5].
Step 10: Mean saturation vapor pressure derived from air temperature(e_{s})
As saturation vapor pressure is related to air temperature, it can be calculated from the air temperature. The relationship is expressed by:
Where,
e_{(T)} = saturation vapor pressure at the air temperature T, kPa
T = air temperature, °C.
Therefore, the mean saturation vapor pressure is calculated as the mean between the saturation vapor pressure at both the daily maximum and minimum air temperatures.
Where,
T_{max} = maximum daily air temperature, °C;
T_{min} = minimum daily air temperature, °C.
The mean saturation vapor pressure for a day, week, decade, or month should be computed as the mean between the saturation vapor pressure at the mean daily maximum and minimum air temperatures for that period:
Step 11: Actual vapor pressure (e_{a}) derived from relative humidity
The actual vapor pressure can also be calculated from the relative humidity. Depending on the availability of the humidity data, different equations should be used.
Where,
e_{a} = actual vapour pressure, kPa;
e_{(Tmin)} = saturation vapour pressure at daily minimum temperature, kPa, [Eq. 17];
e_{(Tmax)} = saturation vapour pressure at daily maximum temperature, kPa, [Eq. 16];
RH_{max} = maximum relative humidity, %;
RH_{min} = minimum relative humidity, %.
Note I:
a) When using equipment where errors in estimating RH_{min} can be large, or when RH data integrity are in doubt, use only RH_{max}:
b) In the absence of RH_{max} and RH_{min}:
Note II: For missing or questionable quality of humidity data, the e_{a} can be obtained by assuming when the air temperature is close to T_{min}, the air is nearly saturated with water vapor and the relative humidity is near 100%, in other words, dewpoint temperature (T_{dew}) is near the daily minimum temperature (T_{min}). If T_{min} is used to represent T_{dew} then:
Step 12: The inverse relative distance EarthSun (dr) and solar declination (
)
The inverse relative distance EarthSun, dr, and the solar declination, ¥, are given by:
Where,
J = number of the day in the year between 1 (1 January) and 365 or 366 (31 December).
Note: to convert date (MM/DD/YYYY) to Julian in Microsoft Excel the following command can be used:
= ((MM/DD/YYYY)DATE(YEAR((MM/DD/YYYY)),1",1")+1)
Step 13: Conversion of latitude (φ) in degrees to radians
The latitude, φ, expressed in radians is positive for the northern hemisphere and negative for the southern hemisphere (see example below). The conversion from decimal degrees to radians is given by:
Example 1: to convert 13º44N to decimal degrees = 13+44/60 = 13.73
Example 2: to convert 22º54S to decimal degrees = (22)+(54/60) = 22.90
Step 14: Sunset hour angle (ω_{s})
The sunset hour angle (…s) is given by:
Where,
φ = latitude expressed in radians, [Eq. 25];
= solar declination, [Eq. 24];
Step 15: Extraterrestrial radiation (R_{a})
The extraterrestrial radiation, R_{a}, for each day of the year and for different latitudes can be estimated from the solar constant, the solar declination and the time of the year by:
Where,
R_{a} = extraterrestrial radiation, MJ m^{2} day^{1};
G_{sc} = solar constant = 0.0820 MJ m^{2} min^{1};
d_{r} = inverse relative distance EarthSun [Eq. 23];
ω_{s} = sunset hour angle, rad, [Eq. 26];
φ = latitude, rad, [Eq.25];
= solar declination, rad, [Eq. 24].
Step 16: Clear sky solar radiation (Rso)
The calculation of the clearsky radiation is given by:
R_{so} = (0.75 + 2E10^{5}z)R_{a} (Equation 28)
Where,
z = elevation above sea level, m;
R_{a} = extraterrestrial radiation, MJ m^{2} day^{1}, [Eq. 27];
Step 17: Net solar or net shortwave radiation (R_{ns})
The net shortwave radiation resulting from the balance between incoming and reflected solar radiation is given by:
R_{ns} = (1  a)R_{s} (Equation 29)
Where,
R_{ns} = net solar or shortwave radiation, MJ m^{2} day^{1};
α = albedo or canopy reflection coefficient, which is 0.23 for the hypothetical grass reference crop, dimensionless;
R_{s} = the incoming solar radiation, MJ m^{2 }day^{1}, [Step 2, Eq. 6];
Step 18: Net outgoing long wave solar radiation (Rnl)
The rate of longwave energy emission is proportional to the absolute temperature of the surface raised to the fourth power. This relation is expressed quantitatively by the StefanBoltzmann law. The net energy flux leaving the earth's surface is, however, less than that emitted and given by the StefanBoltzmann law due to the absorption and downward radiation from the sky. Water vapor, clouds, carbon dioxide, and dust are absorbers and emitters of longwave radiation. It is thereby assumed that the concentrations of the other absorbers are constant:
Where,
R_{nl} = net outgoing longwave radiation, MJ m^{2} day^{1},
σ = StefanBoltzmann constant [4.903 10^{9} MJ K^{4 }m^{2} day^{1}],
T_{max} = K maximum absolute temperature during the 24hour period [K = °C + 273.16],
T_{min} = K minimum absolute temperature during the 24hour period [K = °C + 273.16],
e_{a} = actual vapor pressure, kPa,
R_{s} = the incoming solar radiation, MJ m^{2} day^{1}, [Step 2, Eq.6];
R_{so} = clear sky solar radiation, MJ m^{2} day^{1}, [Step 16, Eq. 28];
Step 19: Net radiation (R_{n})
The net radiation (R_{n}) is the difference between the incoming net shortwave radiation (R_{ns}) and the outgoing net longwave radiation (R_{nl}):
R_{n} = R_{ns}  R_{nl} (Equation 31)
Where,
R_{ns} = net solar or shortwave radiation, MJ m^{2} day^{1}, [Step 17, Eq. 29];
R_{nl} = net outgoing longwave radiation, MJ m^{2} day^{1},[Step 18, Eq. 30].
To express the net radiation (R_{n}) in equivalent of evaporation (mm) (R_{ng});
R_{ng} = 0.408 X R_{n} (Equation 32)
Where,
R_{n} = net radiation, MJ m^{2} day^{1}, [Eq. 31];
Final Step: Overall ET_{o} equation
FS1. Radiation term (ET_{rad})
ET_{rad} = DT X R_{ng} (Equation 33)
Where,
ET_{rad} = radiation term, mm d^{1};
DT = Delta term, [Step 7, Eq. 12];
R_{ng} = net radiation, mm, [Eq. 32]
FS2. Wind term (ET_{wind})
ET_{wind} = PT X TT (e_{s}  e_{a}) (Equation 34)
Where,
ET_{wind} = wind term, mm d^{1};
PT = Psi term, [Step 8, Eq. 13];
TT = Temperature term, [Step 9, Eq. 14];
e_{a} = actual vapor pressure, kPa, [Step 11, Eq. 19];
e_{s} = mean saturation vapor pressure derived from air temperature, kPa, [Step 10, Eq. 15];
Final Reference Evapotranspiration Value (ET_{o})
ET_{o} = ET_{wind} + ET_{rad} (Equation 35)
Where,
ET_{o} = reference evapotranspiration, mm d^{1};
ET_{wind} = wind term, mm d^{1};
ET_{rad} = radiation term, mm d^{1};
The step by step process of reference evapotranspiration calculation was given in this document. Values of evapotranspiration are largely determined by climatic conditions which are available in the FAWN system (http://fawn.ifas.ufl.edu/). The PenmanMonteith ET estimation detailed has been shown to be the most accurate for Florida conditions, and it can be applied on a daily basis for better irrigation management or other water resources applications.
1 mm = 0.03937 in
1 mm d^{1} = 2.45 MJ m^{2} d^{1}
1 J cm^{2} d^{1} = 0.01MJ m^{2} d^{1}
1 calorie = 4.1868 J
1 cal cm^{2} d^{1} = 4.1868 * 10^{2} MJ m^{2}d^{1}
1 W = 1 J s^{1}
1W m2 = 0.0864 MJ m^{2}
°C = (°F –32) 5/9
Kelvin (°K) = (°C) + 273.16
1 millibar (mbar) = 0.1 kPa
1 bar = 100 k Pa
1 cm of water = 0.09807 kPa
1 mm of mercury (mmHg) = 0.1333 kPa
1 atmosphere (atm) = 101.325 kPa
1 lb/in^{2} (psi) = 6.896 kPa
1 kilometer day0 (km d^{1}) = 0.01157 m s^{1}
1 ft s^{1} = 0.3048 m s^{1}
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Allen, R. G., Walter, I. A., Elliot, R. L., Howell, T.A., Itenfisu, D., Jensen, M. E. and Snyder, R. 2005. The ASCE standardized reference evapotranspiration equation. ASCE and American Society of Civil Engineers.
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Boman, B.J., and E.W. Stover. 2002. Outline for Managing Irrigation of Florida Citrus with High Salinity Water. AE217. Gainesville, University of Florida Institute of Food and Agricultural Aciences, http://edis.ifas.ufl.edu/pdffiles/ae217 Accessed Dec 8, 2009.
Dukes, M.D., M.L. Shedd, and S.L. Davis. 2009. Smart irrigation Controllers: Probramming Guidelines for EvapotranspirationBased Irrigation Controllers. AE445. Gainesville, University of Florida Institute of Food and Agricultural Aciences, http://edis.ifas.ufl.edu/pdffiles/ae445 Accessed Dec 8, 2009.
Howell, T. A. and Evett, S. R. 2006. The PenmanMonteith Method. Available online: http://www.cprl.ars.usda.gov/wmru/pdfs/PM%20COLO%20Bar%202004%20corrected%209apr04.pdf. Accessed December 1st, 2009.
Irmak, S., and D.Z. Haman. 2003. Evapotranspiration: Potential or Reference? ABE 343. Gainesville: University of Florida Institute of Food and Agricultural Sciences, 2003. http://edis.ifas.ufl.edu/pdffiles/AE/AE25600.pdf Accessed Aug 04, 2008.
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Values for C_{n} and C_{d} in Eq. 4 (after Allen et al. 2005).
Calculation time step 
Short reference crop ET_{o s} 
Tall reference crop, ET_{r s} 
Units for ET_{os},ET_{rs} 
Units for R_{n} and G 

C_{n} 
C_{d} 
C_{n} 
_{ }C_{d} 

Daily 
900 
0.34 
1600 
0.38 
mm d^{1} 
MJ m^{2}d^{1} 
Hourly, daytime 
37 
0.24 
66 
0.25 
mm h^{1} 
MJ m^{2} h^{1} 
Hourly, nighttime 
37 
0.96 
66 
1.7 
mm h^{1} 
MJ m^{2} h^{1} 
Note that ET_{sz} for a short crop (ET_{os}) equation is identical to the FAO56 PenmanMonteith equation previously described [Eq. 3]. FAO 56 equation has been selected because it closely approximates grass ET_{o} at the location evaluated, is physically based and explicitly incorporates both physiological and aerodynamic parameters. FAO56 PenmanMonteith equation has been widely use for Florida conditions. Moreover, procedures have been developed for estimating missing climatic parameters (Allen et al. 2005; Romero et al. 2009). The objective of this publication is to provide a stepbystep calculation of the reference evapotranspiration (FAO56 method) for a given location from the available weather data. 

Where, ET_{o} = reference evapotranspiration, mm day^{1}; R_{n} = net radiation at the crop surface, MJ m^{2} d^{1}; G = soil heat flux density, MJ m^{2} d^{1} T = mean daily air temperature at 2 m height, °C; u_{2} = wind speed at 2 m height, m s^{1}; e_{s} = saturation vapor pressure, kPa; e_{a} = actual vapor pressure, kPa; e_{s}e_{a} = saturation vapor pressure deficit, kPa; = slope of the vapor pressure curve, kPa °C^{1} = psychrometric constant, kPa °C^{1} 
Required inputs for ET_{o} calculation.
Symbol 
Parameter 
Unit 
T_{max}^{a} 
a maximum temperature 

T_{min}^{a} 
a minimum temperature 

RH_{max}^{a} 
maximum relative humidity 
% 
RH_{min}^{a} 
minimum relative humidity 
% 
R_{s} 
average solar radiation 
MJ m^{2} d^{1} 
U_{2} 
average wind speed 
m s^{1} at h ^{b} m 
P 
atmospheric pressure (barometric) 
kPa 
Z 
site elevation above sea level 
m 
J 
Julian day 
 
LAT 
Latitude 
degree 
^{a} values obtained in the period of 24h (0:00:01 AM to 11:59:59 PM). ^{b} h = height of measurement above ground surface in meters. 
This document is AE459, one of a series of the Agricultural and Biological Engineering Department, UF/IFAS Extension. Original publication date February 2010. Revised August 2015. Reviewed August 2018. Visit the EDIS website at http://edis.ifas.ufl.edu.
Lincoln Zotarelli, assistant research scientist; Michael D. Dukes, associate professor; Consuelo C. Romero, postdoctoral researcher; Kati W. Migliaccio, assistant professor, Department of Agricultural and Biological Engineering; and Kelly T. Morgan, assistant professor, Department of Soil and Water Science; UF/IFAS Extension, Gainesville, FL 32611.
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U.S. Department of Agriculture, UF/IFAS Extension Service, University of Florida, IFAS, Florida A & M University Cooperative Extension Program, and Boards of County Commissioners Cooperating. Nick T. Place, dean for UF/IFAS Extension.