GLOBAL PATTERNS OF THE CLIMATIC ELEMENTS:

(1) SOLAR ENERGY(Linked to solar insolation

& R, net radiation)

CONTROLS OF SOLAR INSOLATION

1) Sun angle (intensity) -- changes with latitude, time of day, time of year

2) Duration (day length) -- changes with latitude, time of year3) Cloud cover

(and general reflectivity of atmosphere)

4) Surface albedo (water, soil, snow, ice, vegetation,

land use)

In general, land areas (with lower atmospheric moisture) receive more insolation than adjacent water areas and thehighest values occur over subtropical deserts.

REVIEW OF INSOLATIO

N

DURATION

INTENSITY

RADIATION / ENERGY BALANCE

Q* = ( K↓ - K↑ ) + ( L↓ - L↑ ) where K↓ = direct + diffuse shortwave

solar radiation

Kiehl and Trenberth (1997) BAMS

Trenberth et al. (2009) BAMS

Radiative Components

Net short-wave radiation = short-wave down - short-wave up

Net long-wave radiation = long-wave down - long-wave up

Net radiation (R net) =

net short-wave radiation + net long-wave radiation

Positive values represent energy moving towards the surface, negative values represent energy moving away from the surface.

Net short-wave radiation =

Positive values represent energy moving towards the surface, negative values represent energy moving away from the surface.

SW absorbed =

Function of INTENSITY &

DURATION & sun angle / albedo

Net long-wave radiation =

Positive values represent energy moving towards the surface, negative values represent energy moving away from the surface.

Net Surplus

Net Deficit Net Deficit

Annual mean absorbed solar radiation,

emitted longwave radiation (OLR) and net radiation by latitude

S = Solar radiation T = Terrestrial radiation

Net Radiation =

Positive values represent energy moving towards the surface, negative values represent energy moving away from the surface.

Non-Radiative Components

Sensible heat flux (H) = direct heating, a function of surface and air temperature

Latent heat flux (LE) = energy that is stored in water vapor as it evaporates, a function of surface wetness and relative humidity

Positive values for sensible and latent heat flux represent energy moving towards the atmosphere, negative values represent energy moving away from the atmosphere. 

Non-Radiative Components

Change in heat storage (G) = net radiation - latent heat flux - sensible heat flux

G = R net - LE - H

Positive values for change in heat storage represent energy moving out of storage, negative values represent energy moving into storage.

Sensible Heat Flux = H

Positive values for sensible and latent heat flux represent energy moving towards the atmosphere, negative values represent energy moving away from the atmosphere. 

Latent Heat Flux = LE

Positive values for sensible and latent heat flux represent energy moving towards the atmosphere, negative values represent energy moving away from the atmosphere. 

Humid Tropical / Equatorial rainforest

Tropical desert

R net

LE

H

R net

LE

H

Tropical wet-dry climate

Grassland /steppe climate

Tropical wet climate

Tropical desert climate

Change in Heat Storage = G

Positive values for change in heat storage represent energy moving out of storage, negative values represent energy moving into storage.

Air Temperature (at the surface) = T (C)Seasonal temperature variations can be explained in terms

of the latitudinal & seasonal variations in the surface energy balance. 

The pattern of temperatures are a function of net short-wave radiation, net long-wave radiation, sensible heat flux, latent heat flux and change in heat storage. 

GLOBAL PATTERNS OF THE CLIMATIC ELEMENTS:

(2) TEMPERATURE                      

CONTROLS OF HORIZONTAL TEMPERATURE PATTERNS

1. Sun angle & Duration

2. Land vs. water thermal contrasts

3. Warm & Cold surface ocean currents

4. Elevation

5. Ice/Snow albedo effects

6. Prevailing atmospheric circulation

1. Sun Angle & DurationSun angle (influences intensity of solar insolation & albedo) Duration (based on day length)

- both change with latitude and time of year

Leads to: zonal (east-west) distribution of isotherms,

hot in low latitudes; cold in high latitudes

  Given the same intensity of insolation, the surface of any extensive deep body of water heats more slowly and cools more slowly than the surface of a large body of land.

4 Reasons:

1) water has a higher specific heat and heat capacity than land

2) transmission of sunlight into transparent water

3) mixing is possible in water, but not soil

4) evaporation cools air over water during hot season (less evap during winter)

Leads to:

• annual and diurnal temperature ranges will be less in coastal/marine locations

• the lag time from maximum insolation to time of maximum temperature may be slightly longer in coastal/marine locations

2. Land vs. water thermal contrasts

3. Warm and Cold Ocean Currents

4. Elevation

5. Ice /Snow Albedo & Other Effects

6. Prevailing atmospheric circulation

Temperatures are affected by the temperature "upwind" -- i.e. where the prevailing winds and air masses originate

MAPPING HORIZONTAL TEMPERATURE PATTERNS

•Isotherms = lines connecting points of equal temperature

•Isotherms will be almost parallel, extending east-west if Control #1 (sun angle) is the primary control.

•If any of the other controls are operating, isotherms on a map will have an EQUATORWARD shift over COLD surfaces and a POLEWARD shift over WARM surfaces

•The TEMPERATURE GRADIENT will be greatest where there is a rapid change of temperature from one place to another (closely spaced isotherms).

Continental surfaces in winter tend to have the steepest temperature gradients.

Temperature gradients are much smaller over oceans, no matter what the season.

JANUARY JULYNorthern Hemisphere

Southern Hemisphere

Southern Hemisphere

Northern Hemisphere

JANUARY JULY

http://geography.uoregon.edu/envchange/clim_animations/

Constructed by:

Jacqueline J. Shinker, “JJ” Univ of Oregon Climate Lab

The NCEP / NCAR REANALYSIS PROJECT

DATASET

http://www.cdc.noaa.gov/cdc/data.ncep.reanalysis.html

The assimilated data are:

-- computed by the reanalysis model at individual gridpoints

-- to make gridded fields extending horizontally over the whole globe

-- at 28 different levels in the atmosphere.

(Some of these levels correspond to the "mandatory" pressure height level at which soundings are taken, e.g., 1000, 850, 700, 500, 250 mb, etc.)

The horizontal resolution of the gridpoints is based on the T62 model resolution (T62 = "Triangular 62-waves truncation") which is a grid of 192 x 94 points, equivalent to an average horizontal resolution of a gridpoint every 210 km.

The pressure level data are saved on a 2.5 latitude-longitude grid. Note that the gridpoints for computed model output are more numerous and much closer together in the mid and high latitudes, and fewer and farther apart over the low latitudes.

Map of locations of Raobs soundings for the globe:

Raobs = rawindsonde balloon soundings

Reanalysis Output Fields The gridded output fields computed for different

variables have been classified into four classes ( A, B, C, and D) depending on the relative influence (on the gridded variable) of:

(1)the observational data

(2) the model

IMPORTANT: "the user should exercise caution in interpreting results of the reanalysis, especially for variables classified in categories B and C." (p 448)

Class A = the most reliable class of variables; "analysis variable is strongly influenced by observed data"

value is closest to a real observation

Class A variables:

mean sea level pressure,

geopotential height (i.e. height of 500 mb surface, 700 mb surface, etc.),

air temperature,

wind (expressed as two vectors dimensions: zonal = u wind (west-east ) and meridional = v wind (north-south),

vorticity (a measure of rotation)

Class B = the next most reliable class of variables

"although some observational data directly affect the value of the variable, the model also has a very strong influence on the output values."

Class B variables:

surface pressure,

surface temperature (and near-surface 2-m

temperature) , max and min temperature,

vertical velocity,

near-surface wind (u & v wind at 10 m),

relative humidity, mean relative humidity,

precipitable water content, and snow cover

Class C = the least reliable class of variables

-- NO observations directly affect the variable and it is derived solely from the model computations

-- forced by the model's data assimilation process, not by any real data.

Class C variables:

precipitation, snow depth, soil wetness and soil temperature, surface runoff, cloud fraction (% high, middle, low), cloud forcing, skin temperature, surface wind stress, gravity wind drag,

and latent and sensible heat fluxes from surface or top of the atmosphere.