Computing leaf wetness term in an apple plantation

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There are accessible hourly recordings of climate radar estimations of precipitation ( pixel zone 1x1km) The issue of moving estimations in the neighborhood

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Slide 1

Computing leaf wetness length in an apple plantation Tor Håkon Sivertsen The Norwegian Crop Research Institute

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The down to earth setting of the issue We are thinking about a little locale with natural product cultivating. A couple mechanized agro meteorological stations are put in the zone The district is secured by a climate radar The issue of evaluating leaf wetness term is firmly associated with plant pathology

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NORSJØ REGION OF SOUTHERN NORWAY secured by two climate radars

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The NORSJØ zone

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The framework for making estimations There are a couple computerized agro meteorological stations in the territory measuring air temperature, precipitation, relative dampness of the air, worldwide radiation, wind speed (2m) and leaf wetness length (hourly recordings) There are accessible hourly recordings of climate radar estimations of precipitation ( pixel zone 1x1km)

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The issue of moving estimations in the neighborhood have four agrometeorological stations and 15 locales with natural product cultivating in the range The estimations of precipitation by radar is associated with every site The estimations at the agro meteorological stations are exchanged to whatever is left of the destinations. We are utilizing the theories of turbulent blending and dry adiabatic procedures as a first guess

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The issue of figuring/measuring leaf wetness in a plantation We take a gander at the procedures of importance Precipitation Condensation of water on the leaves Evaporation Dry surface of the leaf

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Precipitation The measure of precipitation is measured at four locales outfitted with agro meteorological stations by utilizing tipping containers , hourly reco rdings We additionally measure precipitation by climate radar i pixel regions of 1x1km, hourly recordings .

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Condensation Using the (exchanged) mesurements of temperature and relative moistness of the air and also the information of the height above ocean level, the relative stickiness of the air at every site is evaluated. While the relative moistness of the air is > 100 % buildup is considered to happen. Estimations of leaf wetness span at the agro meteorological stations enlighten us something concerning the length of this procedure in the range.

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Evaporation In the figuring we are utilizing the parameters 'Stockpiling limit' and 'Real stockpiling of water on the leaf' These parameters may later on be changed by our hourly estimations of 'leaf wetness length' In the methodology we consider the water adjust

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Calculating Evaporation of blocked water This procedure is imperative and troublesome and the approach is associated with the vitality adjust and the water adjust

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The general issue of neighborhood climate - How to distinguish the nearby climate? - How to extrapolate estimations when knowing the physical components? - What about shift in weather conditions? - What about displaying?

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Adiabatic turbulent blending of air The method for evaluating parameter values at a site "j" when knowing the deliberate parameter values at an agro meteorological station "i" is associated with the theories of turbulent adiabatic blending of packages of air in the limit layer near the ground. We get the dry adiabatic slip by rate: T(z i )- T(z j )=-(g/c dad )( z i - z j ) g: The increasing speed of gravity T(z): The air temperature 2m over the dirt surface c dad : The warmth limit of the air at consistent weight z i : The stature above ocean level of a site indicated by the record "i"

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Adiabatic turbulent blending of air We likewise know the relative stickiness of the air RH(z i ) and the air temperature T(z i ) at the site 'i', and we may figure e w (T(z i )), the immersion vapor weight and e(z i ), the water vapor weight of the air. e w (T(z)): The immersion water vapor weight at the temperature e(z): The water vapor weight of the air at the level "z" We expect that the water vapor noticeable all around furthermore the dry air might be displayed by the perfect gas law at the site "i" where p ai α ai = R a T e i α vi = R v T α a : The particular volume of the dry air  α v : The particular volume of the water vapor

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Adiabatic turbulent blending of air We are utilizing Poisson's condition to compute the change of aggregate weight in (an adiabatic procedure of turbulent blending of air bundles) from the site "i" to the site 'j': (T i/T j ) · ( p i/p j ) κ =1 κ= R a/c p By utilizing the segment of the halfway weights and the incomplete densities of the air, and utilizing the above recipes we may discover the water vapor weight e(z ) and the immersion weight of water vapor at the site 'j', knowing the thermodynamic properties at the site 'i'. p i =p ai + e i ρ j = ρ aj + ρ vj In this framework the weight is not measured, we along these lines need to put p i equivalent to some helper esteem "P" initially.

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Precipitation is measured by climate radar (hourly values) in pixel ranges of 1x1km

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Thank you in particular!