Ebio Ch. 2 Part 2

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Proximity to oceans, mountains, and vegetation can influence climate at a

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regional (e.g. sub-continental) scale

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Heat capacity (energy needed to raise the temperature) of Earth’s surface is higher for

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water than for land

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Regions near large bodies of water (oceans) have cooler temperatures

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in the summer, and warmer temperatures in the winter (heat storage of water)

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Oceans also source of moisture for

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humidity and clouds

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Maritime climate characterized by relatively small

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seasonal temperature change & higher humidities

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Continental climate associated with center of large continents (Asia & N. America) in the temperate zone

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large seasonal changes in temperature

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Heat capacity of air at higher elevations is

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lower, due to fewer air molecules (lower density); radiational heating of the air by the surface is therefore less effective

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Mountains intercept air masses, and force them to rise and cool, leading to higher precipitation on

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windward side, and a drier climate on the leeward side = Rain shadow effect

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Differential heating of slopes can enhance

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storm formation

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Amount of sunlight reflected by the Earth surface (albedo) is determined by the

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color- snow, light colored soils, and grasslands are good reflectors, and have high albedo

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Forests are relatively dark, and have

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low albedo (high absorption of solar radiation)

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Vegetation also enhances water movement from

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soil to the air

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transpiration

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evaporation of water from inside leaf to air + evaporation= evapotranspiration), which is a cooling process

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Vegetation influences how effectively heat is removed by wind (sensible heat loss)

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surface roughness; smooth surface (e.g. grassland) loses heat more effectively than a rough surface (mixed-age forest)

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Climate cycles occur at

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daily, seasonal, decadal, and even 100,000+ year scales

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Climate variation is associated primarily with changes in the amount of

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solar radiation received at Earth’s surface

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Seasonality of climate in the temperate and polar zones is associated primarily with

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changes in temperature

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Seasonality in the tropics is associated primarily with

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changes in precipitation

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The zone of maximum heating and therefore maximum uplift (Intertropical Convergence Zone, ITCZ) and storm formation changes

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seasonally

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Seasonal changes in some temperate and polar lakes associated with

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layering (stratification) of waters

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Water is most dense at

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4 °C

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surface layer (epilimnion) in summer is uniformally

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warm

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deeper, most dense layers (hypolimnion) uniformally

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cold

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intermediate layer (thermocline) is zone of

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temperature change

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Lack of mixing between top and bottom is important for

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nutrient cycling and oxygen supply

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Decadal Changes in Climate
examples include

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El Niño Southern Oscillation (ENSO), Pacific Decadal Oscillation (PDO), and the North Atlantic Oscillation (NAO)

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Decadal Changes in ClimateAssociated with changes in

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atmospheric circulation and high/ low pressure cells

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ENSO occurs when equatorial Pacific easterly trade winds, and associated

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ocean currents, weaken

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El Niño conditions last for around

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18 months, and cycle at 3-8 year intervals

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Long-term (100,000+) year cycles in climate are associated with variations in

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Earth’s orbit

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Glacial-interglacial periods have occurred repeatedly over the last

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3 million years, with glacial periods lasting around 80,000 years, and interglacial (warmer) periods lasting 20,000 years

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Shape of Earth’s orbit and tilt of its axis change with

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time known as Milankovitch cycles

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Milankovitch cycles--orbital shape changes from elliptical, to more circular on 100,000 year time scales

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influences seasonal amount of solar radiation received

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Milankovitch cycles--Tilt of Earth’s axis changes on 41,000 year time cycle- larger angle of tilt accentuates

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the seasonal change in temperature

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Milankovitch cycles--orientiation of the axis relative to other celestrial bodies (wobble) changes at 22,000 year cycles- influences

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Earth-sun distance during the seasons