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Atmosphere

Atmosphere. Part II Moisture. Contents. Hydrological Cycle Three States of water Humidity Adiabatic Processes Condensation Precipitation World distribution of precipitation. Hydrological Cycle.

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Atmosphere

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  1. Atmosphere Part II Moisture

  2. Contents • Hydrological Cycle • Three States of water • Humidity • Adiabatic Processes • Condensation • Precipitation • World distribution of precipitation

  3. Hydrological Cycle • It is the global circulation of moisture (and heat) between the land and seasurface and the atmosphere.

  4. Hydrological Cycle • It is composed of a series of stores or compartments in which moisture is held in various forms and amounts, and a sequence of transfers and transformations of moisture between and within the different stores. • The most important storage is the ocean, sea, lakes and rivers.

  5. Hydrological Cycle - Terms • Water evaporate from water bodies and land surface. • Atmosphere • Vapour is temporarily locked up as gigantic atmospheric storage. • As temperature drops, it condenses (around condensation nuclei) into different forms of precipitation – solid state (snow, hail), liquid state (rain, drizzles, showers) and semi-gaseous state (fog and mist). • Land surface and vegetation • Snow on mountain tops or in high latitudinal zones, which is stored temporarily until spring thaw. • With temperature rising, it melts into water. • Rain falls through leaves of various vegetation types at different rates through interception and through fall. • Droplets may stay on leafs and stems surface to be evaporated into atmos. Later. • Underground water will be absorbed by roots of vegetation and through transpiration to back into atmos.

  6. Hydrological Cycle - Terms • Underground • When soil is dry (permeable), waterpercolates into soil as infiltration, and is stored below the water table as underground water. • The water flow of this subsurface water is called return flow which reaches rivers as surface water. • If infiltration is checked (few vegetation or saturated soil), water flows on land surface as surface runoff. • Some water will be used for domestic, industrialconsumption and farming. Water quality may be down grade by pollution. • Evapotranspiration brings water from various water storage back to the atmos. again in the form of water vapour.

  7. Hydrological Cycle

  8. Hydrological Cycle

  9. Three States of water Exchanges of heat energy between 3 states of water is called latent heat.

  10. Humidity • The ability of the air tohold water vapourdepends solely on temperature. • A mass of air is holding the maximum amount of water vapour possible at a given temperature (dew point temperature), it is said to be saturated. • Less than the maximum amount is said to be unsaturated. • Holding more, it is known as supersaturated.

  11. Absolute Humidity • It refers to the actual quantity of moisture present in the air. (gram/m3)

  12. Relative Humidity • The proportion of water vapour present relativeto the maximum quantity, expressed as percentage (%) • The change in relative humidity can be caused by: • Increase water vapour amount (evaporation, transpiration, sea breeze…..) • Changes of temperature.

  13. Relative Humidity • Relative humidity reaches 100%, it is saturated. Further cooling will cause condensation of the excess vapour into liquid form. • The temperature at which condensation takes place is known as dew point temperature.

  14. Adiabatic Processes • Adiabatic means that there is no heat exchange between the air parcel and its surroundings environment. • The process of adiabatic depends on parcels of air rising through the atmosphere to higher elevations. (expansion cooling) • Air may be induced to rise by convection, orographic uplift, turbulence in the air flow, and uplift at frontal surfaces. • The decrease of pressure with height allows the rising air parcel to expand. (loss heat – cooling) • When a air parcel moving to lower level, it gains heat by contraction. • Expansion energy is used up temp. decrease

  15. Adiabatic Cooling

  16. Dry & Wet Adiabatic Lapse Rate • Dry Adiabatic Lapse Rate (DALR): • Relative Humidity below 100%, adiabatic cooling and warming takes place at a fixed rate (-10oC/1000m) • Saturated Adiabatic Lapse Rate (SALR): • It is lower than the DALR for latent heat was released into air, which offsets the adiabatic temperature loss. -(5~6)oC/1000m)

  17. Adiabatic Lapse Rate and Environmental Lapse Rate • Adiabatic Lapse Rates • The temperature changeswith height of a air parcel which rising or subsiding. • Environmental Lapse Rate • The actual environmental temperature changes with height (-6.5oC/1000m)

  18. Adiabatic Lapse Rate and Environmental Lapse Rate

  19. Condensation • Condensation is the direct cause of all the various forms of precipitation. • Conditions for condensation: • Air temperature drops to dew point temp. but its volume remains constant • Volume of the air parcel expands. (adiabatic cooling) • Joint functions of above two causes, which reduces the moisture-holding capacity of the air. • Condensation will be accelerated by the presence of condensation nuclei / hygroscopic nuclei (dust, salt, smoke,……)

  20. Forms of Condensation • Dew and Frost • Mist and Fog • Advection Fog • Radiation Fog • Clouds

  21. Dew and Frost • Dew consists of relatively large water droplets which (condense) collect or deposit on cold or cool surface under clam conditions. • Frost consists of ice crystals condense on a cold or cool surface, but the dew point temp. is below 0oC. Water vapour transform to ice crystals directly through sublimation process.

  22. Mist and Fog • Mist and fog are very fine condensed water dropletssuspended in lower level of air. • Visibility • Mist < 1000m • Fog > 1000m • They are usually formed by advection of warm, moist air (advection fog) and by intense radiation at night (radiation fog). • Condensation nuclei are very important for their formation.

  23. Advection Fog • The lower layer of warm air is cooledbelow dew point temp. by contact with cooler air or surface. • Formation conditions • Warm, moist air passes over a cooler land or sea surface horizontally. • Cold and warmocean currents meet each other • Warm moist air (may be from ocean) merges with cool dry air (may be from land), which is also called frontal fog. • It is very common in spring in HK. • It will be vanishduring the day time when appears and temperature rises.

  24. Advection Fog

  25. Radiation Fog • Moist air is cooled for heat loss from ground by radiation • It occurs in cold weather when the sky is clear, clam and stable condition. • It is common in winter and in the industrial regions

  26. Clouds • Clouds consist of extremely tiny water droplets or minute ice crystalssuspended in upper level air. • The formation is the same of those of fog. • Favourable formation conditions • Air temperature fall down to dew point for form water droplets or ice crystals. • Presence of condensation nuclei • Water in such minute quantities can remain liquid form far below 0oC without condensation nuclei, it is said supercooled water (-12oC to -30oC).

  27. Classification of Cloud Types • It can be classified on two characteristics: Form (Stratiform and cumuliform) and Altitude. • Stratiform: • They are blanket like, often covering vast areas, but are fairly thin comparison to horizontal dimensions. • Cumuliform: • They tend to display a height as great as their horizontal dimensions. • Cumulus is a white, wool pack cloud mass, showing a flat base and a head of cauliflower. • Cumulonimbus is the thunderstorm cloud mass of enormous size which brings heavy rainfall, thunder and lightning, and gusty winds. It extend from a height of 300 to 600m at the base up to 9000 to 12000m.

  28. Altitude

  29. Stratus

  30. Cumulus

  31. Cumulonimbus

  32. Cloud types (low to middle Level)

  33. Cloud types (High Level)

  34. Stability and Precipitation • Air Stability • Absolute instability • Conditionally stable (conditionally unstable) • Absolute stability • Highly stable (Inversion) • Formation of precipitation • Forms of precipitation • Types of rainfall • Convectional precipitation • Orographic precipitation • Cyclonic precipitation

  35. Air Stability • It is determinedby the relationship between the environmental lapse rate (ELR) and the dry and saturated adiabatic lapse rate (DALR and SALR). • It is a very important meteorological phenomenon because it influences the amount and the type of condensation (clouds, fog….), together with other related weather phenomena, such as rain and hail…...

  36. DALR and SALR

  37. ELR and ALR

  38. Absolute instability • Definition: • When uplifted air is encouraged to rise still further and descending airis continued to sink. • Environmental lapse rate is greater than that of both dry and wet adiabatic lapse rates. ELR > DALR >SALR

  39. Conditionally Stable / Unstable • Definition: • Environmental lapse rate is less than the dry but greater than the saturated adiabatic lapse. • DALR > ELR > SALR

  40. Absolute Stability • Definition: • A vertically displaced air parcel tends to return to itsoriginal position. • DALR > SALR > ELR

  41. Highly Stable Air (Inversion) • Definition: • When the environment air temperature increasewith altitude, temperature inversion exist. • It effectively put a cap on the atmosphere.

  42. Formation of Precipitation • Four conditions for precipitation • a) Cooling air • b) Condensation and cloud formation • c) Accumulation of moisture • d) Growth of cloud droplets • When clouds form, they are 99.9% non-precipitating. • Stages (c) and (d) are fundamental in precipitation production. • Stages (d) is the most critical one in precipitation formation. It is because the water droplets and ice crystals of clouds have to be transformed intoheavier particles. • There are 2 main mechanisms to increase size of cloud droplets for precipitation.

  43. Collision Mechanism • Rising and sinking air motions within cloud carry with different size of droplets of ice-crystals. • The larger droplets tend to catch more of the smaller cloud particles and grow. • When two liquid water droplets collide and join together the process is called coalescence. • The conjoining of two ice crystals is known as aggregation. • An ice crystal collects a water droplet, this process is known as accretion. • Rainfall largely results from coalescence, snowfall from aggregation and hail from accretion.

  44. Collision / Direct capture

  45. Ice-crystal / Bergeron Method • Although supercooled water droplets and ice crystals can co-exist within a cloud, they are unstable and liquid water droplets will evaporate. • The evaporated vapour then condenses and freezes onto the ice crystals surface and ice crystals grow into large snowflakes. • In the tropics areas, raindrops grow by collision processes. • Ice-crystals method is responsible for extra-tropical latitudes(strong convection) and heavy rainfall of mid-latitude areas.

  46. Bergeron Method

  47. Forms of Precipitation • Rain: • When cloud droplets are caused to coalesce into drops too large to remain suspended in the air, rain is formed. • Drizzle: • The diameter of falling rain drops less than 0.5mm. • Sleet: • A mixture of rain and snow • Snow: • Falling ice crystals which grows directly from water vapour to solid form (dew point temp. below 0oC) • Hail: • It consists of rounded lumps of ice, having an internal structure of concentric layers.

  48. Types of rainfall • Convectional Rain • Orographic / Relief Rain • Cyclonic / Frontal Rain

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