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7/27/2019 hidroloji_yagis

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YAI

2. BLM


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Yan Meydana gelmesi iin

gerekli koullar;

1. Havannsoumas

2. Younlamann olmas

3. Yeryzne debilecekirilikte damlalarn olumas

4. Atmosferin o blgesinde yeterlisu buhar olmas


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KMLS YAMUR BULUTLARI KMLO-NMBS YAMUR BULUTLARI

(http://www.windows.ucar.edu/ )

YKSEK VE ORTA YKSEKLKTEK BULUTLAR

BULUTLAR
http://www.windows.ucar.edu/http://www.windows.ucar.edu/


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Yan Oluum mekanizmasna gre trleri

z Konvektif Yalarz Orografik Yalarz Cephesel (Siklonik, Depresyonik) Yalar


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Konvektif Yalar

Nemli havasnarak ykselir

Ykselen hava ktlesi sour,nem younlar.


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Orografik Yalar

Scak ve nemli hava

Daengelini amak iin ykselir ve sour


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Cephesel (Siklonik, Depresyonik) Yalar

Scak Cephe Yalar

Souk Cephe Yalar

Scak hava ktlesi soukhava ktlesini iterken dahaaz youn olduundanykselerek sour..

Souk hava ktlesi scak havaktlesini iterken ok younolduundan kamaeklinde altasokulur. Scak hava kamann

zerinde ykselerek sour..


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YAIIN LLMES

HELMAN PLVOMETRES

1. Plviometreler

2. Plviograflar (Yazcl)Tartl

amand

ral

Devrilen koval

3. Radarlar

4. Uydular(Aratrma dneminde)


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Standart plviometre

This gage is called the SRG, or Standard Rain Gage. This is the mostcommon form of non-mechanical rain gages used for official

measurements for the National Weather Service.

http://www.crh.noaa.gov/ind/coop.htm


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Tartl Plviograf


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Alter perdeli pluviograf

Pluviografn etrafn evreleyen hareketli perdeler rzgar estiinde vakum yaratr.Oluan bu vakum rzgar etkisini (trblans etkilerini) minimuma indirerekyan daha salkl llmesini salar.

http://www.crh.noaa.gov/ind/coop.htm


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RADAR

http://weather.noaa.gov/radar/


14/36

Radar ekoiddeti ve renk kodlar

z DBZ Decibel

The dBZ values increase as the strength of the signal returned to the radar increases. Eachreflectivity image you see includes one of two color scales. One scale (far left) represents dBZvalues when the radar is in clear air mode (dBZ values from -28 to +28). The other scale (near

left) represents dBZ values when the radar is in precipitation mode (dBZ values from 5 to 75).Notice the color on each scale remains the same in both operational modes, only the valueschange. The value of the dBZ depends upon the mode the radar is in at the time the image wascreated.

The scale of dBZ values is also related to the intensity of rainfall. Typically, light rain is occurringwhen the dBZ value reaches 20. The higher the dBZ, the stronger the rainrate. Depending onthe type of weather occurring and the area of the U.S., forecasters use a set of rainrates whichare associated to the dBZ values.


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Radarlar ile verilen hizmetler

Herhangi bir noktaya herhangi bir anda ka mm ya dt,

belirli bir sre zarfnda toplam ya miktar,

Ya baladktan sonraki 30-60 dakikalk sre ierisinde ne kadardaha yan decei tahmini

Herhangi bir noktada ve herhangi bir anda ya tipinin ne olduu(120 km doppler modunda) ve bu yal sistemin hangi yne doruhareket edecei


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Trkiyedeki Radar Kaplamas

Zonguldak

BalkesirAnkara

378 m

1108 m

1807 m

642 m

stanbul

Ankara, Elmadalesinde,

stanbul, Bykkukaya Tepesi, atalca nn 35 km kuzeyinde

Zonguldak, Ac

su tepesi, Zonguldak

n gneyinde, Ereli- Devrek aras

ndaBalkesir, Akaldede Tepesi, Balya ilesi yaknlarnda, Balkesirin batsnda


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Balkesir RadarC-Band Doppler Meteoroloji Radar

Mart 2003 y

l

nda iletmeye al

nm

t

rBalikesir (Akcaldedesi Tepesi)Ykseklik : 642mEnlem : 39 44 26 NBoylam : 27 37 10 EKule :20m , elik KonstrksiyonFirma : Mitsubishi - Japonya


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Uydular


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Gne , Atmosfer Yerkre arasndakielektromanyetik enerji transferi


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Uydu grntleri


21/36

Kar

n llmesiz Kar yann llmesi (Plviometre ve

Plviograflarla)z Kar rtsnn llmesi


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Kar rtsnn llmesi

Kar rtsnn dalmnetkileyen parametreler

EimYnYkseklik

evre koullar (viewfactor).Dier yzeylerdenyanstlan enerji.Yeryzeyinden gelen uzundalga emisyonu, vb.Rzgar etkisi.


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Kar rtsnn llmesi

1.Kar izi yntemi

2.Kar yastklar

3.Gama n lme


24/36

Kar izi almalar

http://snobear.colorado.edu/Markw/SnowHydro/Measuring_Snow/snow_measuring.html#belfort


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Kar rts lm


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Kar ykseklii ve kar su edeer haritalar

http://www.nohrsc.nws.gov/interactive/html/map

Snow depth for 2004 April 16, 4:00 ZSnow water equivalent for 2004 April 16,


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Kar yastklar ve totalizatr

http://snobear.colorado.edu/Markw/SnowHydro/Measuring_Snow/Snotel/snotel.html

The pillow, made of rubber, steel, hypalon, etc, is filled with an antifreeze solution (50/50 mix of water andethanol with flouresceine dye to make it a flourescent green). As the snowpack accumulates on the pillow,it increases the fluid pressure (obviously as this is a quasi closed system) within the pillow.


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Kar yast istasyonu


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Uzaktan alglama yntemleri ile kar lm

NOAA-15 1.6 Micron Channel

http://snobear.colorado.edu/Markw/SnowHydro/Remote/


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Landsat Thematic Mapper (TM)z 30 m spatial

resolutionz 185 km FOVz Spectral

resolution1. 0.45-0.52 m2. 0.52-0.60 m3. 0.63-0.69 m

4. 0.76-0.90 m5. 1.55-1.75 m6. 10.4-12.5 m7. 2.08-2.35 m

z 16 day repeatpass


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Discrimination between Snow and GlacierIce, tztal Alps

Landsat TM, Aug 24, 1989 snow ice rock/veg


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Snow Measurement Airborne Snow Survey Program

Natural Gamma Sources

238

U Series,232

Th Series,40

K Series

Soil

Snow

Atmosphere

Radon Daughtersin Atmosphere

Cosmic Rays

Uncollided

Gamma RadiationAbsorbed by Water

in the Snow Pack

Gamma Radiationreaches

Detector in Aircraft

Scattering


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Airborne Snow Survey Products


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Kar erime modelleri

z TEMPERATURE-INDEX METHODSz M = Mf (Ta - To)

z M = snowmelt (mm/day)z Mf = degree day factor (mm/degreeC/day)z Ta = air temp (degrees C); daily mean, daytime mean, maximum daily Ta; user must decidez To = threshold or base temperature (degreesC) above which snow melt occurs, usually 0 degreesC.

z range is usually 1 mm/degreeC/day < Mf < 7 mm/degreeC/dayz The degree-day factor is the heart of the approach.z The degree-day factor must be calibrated for each basin and may change with elevation on the

same time step and over time at the same point within a basin.z Snowmelt Runoff Model (SRM) developed by Martinec and Rangoz Q = [C a T S ) + P] A

z Q = dischargez c = runoff coefficient; essentially runoff efficiency or what fraction of snowmelt gets converted to discharge.

Calibrate for each basin.z a = degree day factorz T = number of degree daysz S = ratio of snow covered area to total area, e.g. how much of the basin has snow to melt.z P = new precipitation which gets added in to the systemz

A = basin areaz T, S, and P need to be measured (or estimated) dailyz a = 1.1 rhos/rhow is the initial estimate if no calibration done, based on the concept that as the

density of snow increases (rhos), albedo decreases and liquid water content increases, leading tomore efficient melt for the same number of degree days.

z This is a model based on empirical calibrations.

http://snobear.colorado.edu/Markw/SnowHydro/Modeling/modeling.html


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Enerji btesi

z Energy balance submodelz calculate the energy balance of the snow surfacez Q = R + G + H + LE + A + dQ/dt

z Q = net energyz R = net radiationz G = ground heat fluxz H = sensible heat fluxz LE = latent heat fluxz A = advected energy (rain-on-snow)z dQ/dt = change in internal snowpack energy

z since a surface has no volume, Q = zero.z we understand snow/atmosphere energy transfers well from first principles, so we can model this part well at a point if we

can measure the meteorological variables.z where this gets tricky is that over a basin of interest, there are usually few meteorological stations. Spatially distributing the

meteorological variables is difficult.z Snowpack Modelz Another difficult problemz We know little about liquid water retention and movementz Essentially, once we melt snow at the surface of the snowpack, we lose track of the snow.

z Snow Depletion Modelz We need to keep track of the change in SCA and SWE over time.z Obviously, as the amount of SCA decreases with time, the same amount of energy per unit area melts less snow because

there is less snow to melt.z There are a number of good methods to estimate changes in SCA with time, including remote sensing measurements and

aerial photography. With this information you can calculate areal depletion curves (linear, exponential, etc).z Again, our ability to estimate changes in the spatial distribution of SWE over time is a challenge.


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Yalekleri a

Dnya Meteoroloji rgtnn nerdii

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