Lecture 12 Precipitation Interception (1) Interception Processes General Comments Controls on Interception Interception in Woodlands Interception in Grasslands Interception by Crops Measurement of Relative Humidity

Interception Interception Loss Water abstracted from gross precipitation by leaves and stems of a vegetation canopy and temporarily stored in its surfaces. Interception Loss Intercepted water lost by evaporation to the atmosphere before reaching the soil surface

General Comments Accounts for much of the variability in evaporation and transpiration between plant species or associations   Precipitation is usually intercepted by: Tree canopy Grass Shrubs Litter Moss Built structures Interception capacity is usually considered to be a fixed amount for a given site:  Canopy Urban During filling and once storage is full, water passes through the canopy and reaches the soil as: Throughfall (TF) Stemflow (SF)

Net Rainfall 1. 2. 3.

Terms to Remember Interception loss: Part of the rainfall intercepted by a plant canopy is evaporated back into the atmosphere and takes no part in the land-bound portion of the hydrological cycle Throughfall: raindrops and snowflakes that fall through gaps in the plant canopy and water which drips from leaves, twigs and stems Stemflow: Water run down the main stem or trunk from twigs and branches to the ground Gross rainfall: rainfall on top of plant canopies Net rainfall: The sum of throughfall and stemflow Negative interception: Water intercepted from fogs and mists that contributes to stemflow

Controls on the amount of interception 1. Vegetation form/structure   Shape Branch/leaf orientation Broad vs. needle leaves Number of leaves/stems Surface texture Flexibility/turgidity/stability 2. Vegetation growth pattern/physiology Seasonal growth Deciduous habit Total biomass Form/structure Age Growth rate Density of stand Leaf Area Index (LAI) 3. Meteorological Conditions   Precipitation intensity and duration --Heavy and long duration precipitation will quickly exceed crown capacity leading to greater TF and SF --Conifers intercept more because they coincide with gentler rain or snow --Often possible to relate/predict losses from total P Phase of precipitation Snow/sleet/rain/hail Wind speed and turbulence Energy balance Albedo related to vegetation type

Additional Points to Note These botanical and meteorological factors generally apply to non-botanical surfaces as well (e.g., urban surfaces)   Strong dependence on meteorological factors allows interception, TF, or SF to be estimated from empirical relations Originally believed that interception losses were balanced by reduced transpiration losses. This is now believed to be incorrect Interception is not an alternate loss, rather an additional one

Interception loss during precipitation event Interception losses are greatest early during a precipitation event   Losses decrease when interception storage is filled Interception ratio: (Interception loss) / (total precipitation)

Interception Loss from Woodlands Generally: deciduous crown closure > conifer crown closure However, conifer stands tend to exhibit higher interception losses because of higher leaf area density  Conifer interception losses: ~25-35% Decid. Interception losses: ~10-30%   Potential reasoning: needle shapes and distributions relative to broadleaves Spatially variable: density of trees (spacing)

Interception losses from grasses/shrubs LAI of mature, homogeneous grass cover is generally much smaller than that of forests   Higher aerodynamic resistance than tall vegetation; thus, less interception loss Grazed or cut grasslands exhibit greatly reduced storage Interception losses vary ~13-26%

Interception losses from agricultural crops Usually evenly spaced plants   Highly dependent on stage of development Depending on LAI

Interception of snow   Difficult to measure and highly variable spatially due to wind redistribution   Idea: snow accumulation on canopy decreases aerodynamic resistance (smooth) Thus, evaporation rates should be lower than for wet canopy Snow often melts, slides, slips, or is blown off of vegetation Studies indicate only ~15% of intercepted snow sublimates or evaporates Snow-stored water can be much greater than water storage – potential for more evaporation is there but energy requirements are not always met

Fog and clouds   Deposition of fine water droplets to vegetated surfaces (e.g., mist, fog, clouds) Too fine to precipitate and would not be collected by rain gauges “Negative interception” Kittredge (1948) More common in mountainous regions and coastal areas Can be a significant addition of moisture to local vegetation Different process than dew, which is temperature controlled condensation of water vapor  

Instrument for measuring air humidity http://www.mtc.com.my/publication/library/drying/fig5.gif

Relative humidity:   Ratio of the actual amount of moisture in the atmosphere to the amount of moisture the atmosphere can hold Therefore, a relative humidity of 100% means the air can hold no more water (rain or dew is likely) Relative humidity of 0% indicates there is no moisture in the atmosphere. eswb = Saturation vapor pressure at Twb (kPa) esdb = Saturation vapor pressure at Tdb (kPa) ed = Vapor pressure (kPa) Elv = Elevation above sea level (m) P = Air pressure (kPa) Twb = Wet bulb temperature (°C) Tdb = Dry bulb temperature (°C)  

Procedure for Calculating Relative Humidity 1. Approximate the air pressure, P in kPa (kiloPascals). If you don't know your elevation, use P = 101.325 kPa. P = 101.325exp(-0.0001184  Elv) 2. Calculate a conversion factor, A. A = 0.00066(1.0 + 0.00115  Twb) 3. Calculate the saturated vapor pressure at Twb. eswb = exp[(16.78  Twb – 116.9) / (Twb + 237.3)]   4. Calculate the vapor pressure, or the partial pressure of water vapor, ed in kPa. ed = eswb – AP(Tdb – Twb) 5. Calculate the saturated vapor pressure at Tdb. esdb = exp [(16.78  Tdb – 116.9) / (Tdb + 237.3)] 6. Finally, calculate the relative humidity, RH, in percent. RH = 100  (ed / esdb)