Transcript Slide 1
Estimating ET Type of method used will be determined by: 1. Type of surface (e.g. open water vs. leaf) 2. Availability of water for evaporation 3. 4. 5. Amount of air-advected energy Free-water and lake evaporation - start with simplest situation, evaporation from an open water body - generally not possible to generate evaporation equations for a lake using meteorological data alone because Aw and )Q/)t vary significantly from lake to lake -annual values exceptions in lakes with residence time < 1 year - theoretical concept of free-water evaporation (FWE) developed: assumes no advection or changes in heat storage - depends only on overlying climate actual lake evaporation can be calculated from FWE for particular lakes.. Water Balance Approach E = W + SWin + GWin - SWout - GWout - ΔV W is SW is surface water GW is ground water ΔV is lake storage change during the period of consideration - in theory simple, in practice not easy.. Energy-Balance Approach E K L G H AW Q / t w v or, by inserting the Bowen ratio K L G AW Q / t E wv (1 B) The energy balance approach has many of the same detractions as the water-balance approach, but with the energy balance, at least we can: a) b) use regional climatic data to estimate some of the radiation components.. Shortwave Radiation K=Kin(1-a) Kin is incoming SW radiation, and a is the albedo of the surface Kin is the amount of SW radiation hitting the ground. It is conceptually thought of as: Kin Kcs ( , J ) f1( , , ) f2 (C) f3 ( F ) Λ= J = day of year β= α = aspect C = fraction of sky covered by clouds F = fraction of sky covered by forest canopy Kin can be measured directly using pyranometers, or an empirical relation can be used: Kin = [0.355+0.68(1-C)]Kcs albedo can also be directly measured, or a constant assumed depending on the surface type. For water, a typically ranges between 0.05 to 0.10, but with low solar angles can be very high (up to 0.6).. Long-Wave Radiation Net long-wave rad is equal to the LW flux coming in from the atmosphere, minus the amount reflected from the surface and the amount radiated from the surface L w at (Ta 27315 . ) w (Ts 27315 . ) 4 where: εw = εat = effective emmisivity of the atmosphere σ = the Stefan-Boltzman constant (1.17x10-7 cal/cm2/day/K4) temperatures are in Celcius εat is a function of humidity and cloud cover and can be estimated as: at (053 . 0.065e )(1 0.4C) 0.5 a ea is 4 Conduction to the Ground In the case of lakes can be considered negligible Water-Advected Energy Aw cw w [wTa ( SWin )Tswin ( SWout )Tswout ( GWin )Tgwin ( GWout )Tgwout ] cw w is average precipitation rate SW and GW are surface and groundwater inflows and outflows (in volume per time per unit area) temperatures are in celcius.. Change in Stored energy cw w Q (V2TL 2 V1TL1 ) AL V is lake volume T is average lake (reservoir) temperature subscripts 1 and 2 are values at start and end of time period AL = Bowen Ratio Use of the Bowen ratio has the main advantage that it eliminates the need for measuring wind speed Summary of Energy Balance Approach - suffers some of the same problems as water balance approach - better suited to longer (7 days +) time periods to get a maximum accuracy of ±5%.. Pan-Evaporation Approach - simple concept...set a “bathtub” out an measure the water loss E=W-(V2-V1) W= V= storage loss measured to high precision Pans generally over-estimate real evaporation and coefficients are applied for correction so that daily free-water evaporation (mm/day) can be calculated as: E fw 0.7[ E pan 0.00064 P pan (0.37 0.00255v pan ) Tspan Ta 0.88 ] αpan = P = atmospheric pressure (mb) vpan is mean wind speed 15 cm above the pan (km/day) Tspan is water surface temperature (EC) ± is plus when Tspan > Ta and minus when Tspan < Ta "αpan is a factor to account for energy exchange at the edge of the pan (see equation 7-40 in text) .36 pan 034 . 0.0117Tspan (35 . 107 )(Tspan 178 . )3 0.0135v0pan Corrections to the evaporative loss are only needed for calculating short-term (e.g. daily) values since the errors cancel out over the long term (e.g. annually).. Moving to the more complex...ET When we consider ET, Transpiration and Interception Loss - Transpiration is evaporation from the vascular system of plants into the atmosphere - transpiration is a physical process (not metabolic) driven by water content gradients - interception loss is that precip that is caught by the canopy and evaporated directly to the atmosphere.. Potential ET Potential Evaporation (PET) is the rate of ET that occurs under the prevailing solar inputs and atmospheric properties, if the surface is fully wet. Actual ET is the amount really removed. PET is a theoretical concept that defines the “drying power” of the climate or local meteorological conditions, but actual ET is affected by: 1. 2. Maximum leaf conductance 3. 4. presence or absence of intercepted water 1. Temperature-based: e.g. Hammond 2. Radiation-based: use net rad, air temp and pressure. E.g. Priestltley and Taylor 3. Combination 4. Pan: uses pan evap as a proxy for short veg ET “Direct” Measurement of ET Water-balance approaches Lysimeters -Artificially enclosed volumes of soil that have a representative vegetative cover, outflows and inflows of water can be measured, and changes in storage can be measured by weighing -accurate for low-lying vegetation, but very difficult for large (e.g. forest vegetation) Soil moisture Balance - Total ET is monitored by precise measurement of rainfall and soil water content throughout the root zone - can be useful for larger vegetation an is more natural than lysimeters, however obtaining accurate soil moisture profiles is difficult.. Land-Area Water Balance - Problems in accurate assessment of components and ensuring storage change is negligable -error associated with storage change is minimal when mostly soil water involved -Review Dingman’s evaporatranspiration chapter’s section on Turbulent Transfer Methods..