CLIMATECLIMATE INFLUENCINGINFLUENCING FACTORSFACTORS OFOF THETHE CARPATHIANCARPATHIAN BASINBASIN THE MOST FUNDAMENTAL DETERMINANT: LOCATION

© is situated in the middle band of the temperate belt , in the true temperate zone , between the northern latitudes 45 °45 ’ and 48 °35 ’ . © Its distance from the is around 1000 km, which insures a mild ocanic climate effect : 1. The North -Atlantic current brings about a 1 -1.5 °C positive anomaly in the mean annual temperatures . This positive anomaly is stronger in the winter half -year and in Transdanubia . The annual course of temperature is more uniform compared to the continental areas , i.e. east of the Danube . 2. Precipitation is greater , its distribution is more uniform due to the increased winter cyclone activity in Transdanubia . Temperate belt True temperate belt Moist Three climatic effect in the Carpathian basin

CONTINENTAL EFFECT OCEANIC EFFECT

MEDITERRANEAN EFFECT Two basic features of the climate of Hungary:

1. transitional 2. basin location

1. The Carpathian basin is locate in the border of three climate regions : © oceanic (Cf ) © continental (Df ) © Mediterranean (Cs ) The climate of Hungary according to the Köppen’s classification (Szelepcsényi, 2009)

C: Warm-temperate climate (mean temperature of the coldest month is between +18°C and -2°C) D: Cold-temperate climate (mean temperature of the coldest month < -2°C, mean temperature of the warmest month > 10°C) a: hot, warm summer b: moderately warm summer f: annual distribution of precipitation is more or less uniform Areal determinants of precipitation : 1. distance from the sea ; 2. height above sea level ; 3. basin effect ;

Hungary: • Distance from the Atlantic ocean • +35 mm/100m

Mean annual total of precipitation in Hungary

Regional variability AVERAGE 600-700 mm/year Minimum: Hortobágy and Körös- angle: 400-480 mm/year Maximum: Alpokalja: > 900 mm/year 2. Primary consequence of the basin effect : protection against wind .

• Every air current enters the basin as foehn wind . • Th eeffect of cyclones weaken and become unpredictable du to the Alps and Dinaric Alps . • Cold breaks involving oriental winds in winter are significantly delayed by the Carpathian Mountains . © The values of the climatic elements vary quasi -concentrically from the edge towards the centre of the basin .

© Pressure centres and air masses forming the weather of large -scale areas are also transitional .

© The so called action centres – developing either over continents (temporary ) or sea surface (permanent ) − are large -scale areas of low or high air pressure , influencing climate of extended regions through cyclones or anticyclones and their air masses that form over these areas . Temperate belt cyclones developing over the area of the so called Icandic air pressure minimum basically affect the weather of Europe. The most known weather action centres in the Northern Hemisphere occur in the Atlantic ocan and Pacific ocean region of Europe and North America. Air pressure action centres of the Northern Hemisphere are as follows:

− Icelandic minimum (formation of cyclones ) − Azores maximum (formation of anticyclones) − Persian Gulf maximum (formation of cyclones ) − Siberian maximum (formation of anticyclones)

Low or high pressure formations developing in the weather action centres and then moving further due to the air currents basically determine the weather of the regions that they pass over. The classification of air masses based on the above criteria is called large- scale weather tipization. SPATIALSPATIAL ANDAND TEMPORALTEMPORAL CHANGESCHANGES OFOF THETHE CLIMATECLIMATE ELEMENTSELEMENTS ININ HUNGARYHUNGARY

SOLARSOLAR RADIATIONRADIATION © 1938: USA: Teller – Gamow: theory of the thermonuclear fusion : Where from the heat of the Sun originates ? Nuceli are +charged ⇒ they repel each other ; when collision , the conditions of fusion : • Maxwell ’s velocity distribution : at given temperature there are atoms , having significantly higher energy then the average ; • Gamow’s tunnel phenomenon : particles repelling each other , can get near to each other by quantum tunneling ⇒ nuclear force link them to one another ; Multiplying these two factors → thermonuclear fusion theory ; • Hans Bethe : two crashing hydrogen nuclei cannot create a stable helium nucleus ; hydrogen fusion can only be cretaed if in the moment of the brief proximity a β -decay also occurs ⇒ the result of the nuclear fusion : heavy hydrogen ; The heat of the Sun is provided by a totality of low probability events , particulraly proton -proton fusion .

General characteristics :

© It does not need intermediary agent for spreading . It is converted into thermal energy in the presence of substances when going through the atmosphere . © It is relatively constant in time : the value of the solar constant is around 136 8 W⋅m-2. Such an amount of energy comes to the upper boundry of the atmosphere from the Sun . © Electromagnetic energy coming from the Sun has a specific spectral wavelengths distribution . © Passing through the atmosphere , the solar radiation is scattered , absorbed or reflected → irradiance coming to the Earth ’s surface has a loss , weakens and its spectral composition is changing . Why is the sky blue?

Why is the sunset red?

Visible light: elektromagnetic radiation, its wavelength range ≈ 380 nm - 760 nm;

Clear colour: it contains only one wavelenght - colour of lasers - sodium lamps (oringe light street lamps) ↑ ↓ - colours of rainbow

In most cases we do not see clear colours; Colour image: it shows that which wavelength in which strength is present; The colour of the Sun;

A Rayleigh scattering If the dispersing particle has much smaller size than the wavelength of the visible light, (<0,2 λ) ⇒ the visible light is scattering both back and forth and sideways ⇒ sideways, the intensity of scattering is half as much and the light is polarized; ⇒ efficacy of scattering is proprtional with 1/λ4 (⇒ violet is scattered 12–14-times more strongly than deep red!) the multiplicator 1/λ4 suppresses red and highlights blue; Meteorological solar radiation parameters

According to Short wave Long wave Global solar spectra : (λ<3.5mm) (λ>10mm) radiation According to PIRANOMETER PIRGEOMETER PIRRADIOMETER direction : ↓ towards 1. Global solar 6. Atmos -pheric 9. Full -down solar radiation back radiation radiation 2. Diff úz sug árzás 3. Scattered solar radiation ↑ towards 4. Reflected 7. Surafce 10. Full -up solar solar radiation irradiance radiation

Balance 5. Short -wave 8. Long -wave 11. Total radiation radiation budget radiation budget budget © The intensity of the solar radiation can be characterized by the amount of heat that is generated when the radiation is absorbed by a perfectly absorbing body. © Radiation is the amount of heat that is generated on a unit area and unit time when the radiation passes through it perpendicularly , if the area completely absorbed the radiation (Unit :W⋅m-2). © Another important characteristics of the solar radiation : sunshine duration . This is the period of the global radiation exceeding 120 W⋅m-2 ( hours ⋅year -1). © Its measurement started at the turn of the 19 -20th century in Ógyalla and Kalocsa using Angstr öm pirheliometer . Since 1965, the central observatory of the solar radiation detection has been operating in Pestl őrinc. Campbell-Stokes instrument measuring sunshine duration Annual course of solar radiation © The amount of the global solar radiation is determined by the latitude and the degree of cloudiness . In HIngary , 3 ° difference in latitude causes 200 -250 MJ ⋅m-2⋅year -1 difference . © The annual course of the astronomically potential global solar radiation adjusted to the height of the Sun shows minimum in December and maximum in July . © The annual course of the actual global solar radiation is similar , its values reach 65% of the potential value in annual countrywide average (deterrent effect of cloud cover ).

© Monthly minimum in north -east 78 MJ ⋅m-2⋅month -1, az Alf öld közep én 97 MJ ⋅m-2⋅hó-1 . © Monthly maximum in wset 620 MJ ⋅m-2⋅month -1, while in the middle of th Great Plain 700 MJ ⋅m-2⋅month -1. Mean monthly sums of the global solra radiation (MJ ⋅m-2), , Budapest, Kecskemét © In accordance with the annual course , the ratio of the diffuse and direct components of the global solar radiation also changes . © The direct /diffuse ratio only 50 -50% even in the clearer summer half -year . © In winter , two /third of the global solar radiation comes from diffuse radiation .

Mean ratios of the two components of the global solar radiation under mean cloudiness, % Daily course of the global solar radiation and its components Areal distribution of the global solar radiation clearly shows a basin character .

Areal distribution of the mean annual sums of the global solar radiation (MJ ⋅m-2) in Hungary Mean annual sums of the global solar radiation (MJ/m2) in Hungary (2000-2009)

Photosynthetically active global solar radiation is of great importance in agricultural and ecological point of view (wavelength range : 380 -710 nm).

Areal distribution of the mean annual sums of the photo- synthetically active global solar radiation (MJ ⋅m-2) in Hungary Some of the short -wave radiation reaching the surface is reflected (albedo ). In accordance with the changes of the physical parameters of the surface , this shows a spedific temporal and spatial dynamics .

forest vineyard, fruity agricultural area meadow, pasture mean

Annual course of albedo (%) in case of different surfcaes . Albedo shows specific areal changes during the winter - and summer half -year .

Mean areal distribution of the expected value of albedo (%) in January, Hungary Mean areal distribution of the expected value of albedo (%) in July, Hungary Short -wave radiation budget is the difference between global solar radiation and reflected short -wave radiation . This parameter shows similar temporal and spatial dynamics than global solar radiation but with smaller values .

Areal distribution of the mean annual sums of the short-wave radiation budget (absorbed radiation) (MJ ⋅m-2) in Hungary © The surface warming from the absorbed short -wave radiation emits long -wave radiation . © Some of this radiation is absorbed by the atmospheric greenhouse gases and is radiated back to the Earth ’s surface . © The difference of the amount of energy radiated by the surface and re -radiated by the atmosphere is the long -wave radiation budget of the surface . © If this radiation budget is added to the short -wave radiation budget , then we receive the total radiation budget of the surface , which determines the energy source of the climate processes . Areal distribution of the mean annual sums of the total radiation budget (MJ ⋅m-2) in Hungary Sunshine duration If the intensity of the solar radiation exceeds 120 W⋅m-2, then it is said that the sun is shining . Unit: hour ⋅year -1. Its maximum is in July , its minimum is in December.

Areal distribution of the mean annual sums of the sunshine duration (hours) in Hungary Annual sums of sunshine hours Always look on the bright side of things!

We finished for today, goodbye! ямарваа нэг зүйлийн гэгээлэг талыг нь үргэлж олж харцгаая өнөөдөртөө ингээд дуусгацгаая, баяртай

让我们总是从光明的一面来看待事 物吧！ 今天的课程到此结束，谢谢！ دد دادا إإ اا اق اق اءاء!! ﻣﻣ اا ذاذا اوم،اوم، وداودا!!