🌦️Atmospheric Science Unit 4 – Atmospheric Thermodynamics
Atmospheric thermodynamics explores how heat, energy, and work interact in Earth's atmosphere. It's crucial for understanding weather patterns, climate change, and the complex processes that shape our planet's environment.
This field delves into key concepts like temperature, pressure, and humidity, as well as fundamental laws of thermodynamics. It examines atmospheric composition, energy transfer mechanisms, and the principles behind weather forecasting and climate modeling.
Thermodynamics studies the relationships between heat, energy, and work in a system
Atmosphere is a complex system composed of gases, water vapor, and other particles surrounding Earth
Temperature measures the average kinetic energy of molecules in a substance
Pressure is the force exerted by the weight of the atmosphere on a unit area
Measured using barometers (mercury or aneroid)
Humidity quantifies the amount of water vapor present in the atmosphere
Relative humidity expresses the amount of water vapor in the air compared to the maximum amount possible at a given temperature
Adiabatic processes occur without heat exchange between a system and its surroundings
Lapse rate describes the rate at which temperature changes with altitude in the atmosphere
Environmental lapse rate (ELR) refers to the actual temperature change with height in the atmosphere
Fundamental Laws of Thermodynamics
First Law of Thermodynamics states that energy cannot be created or destroyed, only converted from one form to another
Expressed as: ΔU = Q - W, where ΔU is the change in internal energy, Q is heat added to the system, and W is work done by the system
Second Law of Thermodynamics introduces the concept of entropy, stating that the entropy of an isolated system always increases over time
Entropy measures the degree of disorder or randomness in a system
Zeroth Law of Thermodynamics defines thermal equilibrium: if two systems are in thermal equilibrium with a third system, they are in thermal equilibrium with each other
Ideal Gas Law relates pressure, volume, temperature, and amount of gas in a system: PV=nRT
P is pressure, V is volume, n is the number of moles of gas, R is the universal gas constant, and T is temperature in Kelvin
Dalton's Law of Partial Pressures states that the total pressure of a mixture of gases is equal to the sum of the partial pressures of each individual gas
Atmospheric Composition and Structure
Atmosphere is primarily composed of nitrogen (78%) and oxygen (21%), with trace amounts of other gases (argon, carbon dioxide, water vapor)
Atmospheric layers are defined by temperature changes with altitude
Troposphere is the lowest layer, extending from Earth's surface to an average height of 12 km
Most weather phenomena occur in the troposphere
Stratosphere extends from the tropopause to approximately 50 km, characterized by increasing temperature with height due to ozone absorption of UV radiation
Mesosphere extends from the stratopause to about 85 km, with temperature decreasing with height
Thermosphere extends from the mesopause upwards, characterized by increasing temperature with height due to absorption of high-energy radiation
Ozone layer in the stratosphere absorbs harmful UV radiation, protecting life on Earth
Atmospheric pressure decreases exponentially with height, as described by the barometric formula
Temperature and Pressure Relationships
Temperature and pressure are fundamentally linked in the atmosphere
Ideal Gas Law (PV=nRT) demonstrates the direct relationship between temperature and pressure, assuming constant volume and amount of gas
Hydrostatic equation describes the balance between the vertical pressure gradient force and gravity in the atmosphere
dP=−ρgdz, where dP is the change in pressure, ρ is air density, g is gravitational acceleration, and dz is the change in height
Pressure decreases with altitude because the weight of the overlying atmosphere decreases
Temperature generally decreases with altitude in the troposphere due to adiabatic cooling as air parcels expand and rise
Dry adiabatic lapse rate (DALR) is approximately -9.8°C/km
Saturated adiabatic lapse rate (SALR) varies with temperature and pressure but is typically around -6°C/km
Moisture and Phase Changes
Water vapor is the gaseous form of water in the atmosphere
Evaporation is the process by which liquid water transforms into water vapor
Requires energy input (latent heat of vaporization)
Condensation is the process by which water vapor transforms into liquid water
Releases energy (latent heat of condensation)
Sublimation is the direct transition from solid (ice) to gas (water vapor) or vice versa
Relative humidity is the ratio of the actual water vapor pressure to the saturation vapor pressure at a given temperature
Saturation occurs when relative humidity reaches 100%
Dew point temperature is the temperature at which air becomes saturated (100% relative humidity) when cooled at constant pressure
Latent heat is the energy absorbed or released during phase changes without a change in temperature
Latent heat of vaporization (evaporation/condensation): ~2.5 × 10^6 J/kg
Latent heat of fusion (melting/freezing): ~3.3 × 10^5 J/kg
Latent heat of sublimation: ~2.8 × 10^6 J/kg
Atmospheric Stability and Instability
Atmospheric stability refers to the atmosphere's resistance to vertical motion
Stable atmosphere suppresses vertical motion, leading to limited convection and generally fair weather
Occurs when the environmental lapse rate (ELR) is less than the saturated adiabatic lapse rate (SALR)
Unstable atmosphere promotes vertical motion, leading to enhanced convection and potentially severe weather
Occurs when the ELR is greater than the dry adiabatic lapse rate (DALR)
Conditionally unstable atmosphere is stable for unsaturated air parcels but unstable for saturated air parcels
Occurs when the ELR is between the SALR and DALR
Inversion layers, where temperature increases with height, strongly suppress vertical motion and indicate a highly stable atmosphere
Stability can be assessed using various indices and parameters
Lifted Index (LI) compares the temperature of a lifted parcel to the ambient temperature at a given pressure level (usually 500 hPa)
Convective Available Potential Energy (CAPE) measures the amount of energy available for convection
Energy Transfer in the Atmosphere
Radiation is the transfer of energy through electromagnetic waves
Solar radiation is the primary energy source for Earth's atmosphere
Earth's surface and atmosphere emit longwave (infrared) radiation
Conduction is the transfer of energy through direct contact between molecules
Important for heat transfer between Earth's surface and the lower atmosphere
Convection is the transfer of energy through the bulk motion of fluids (air in the atmosphere)
Convection currents are driven by buoyancy differences due to temperature and density variations
Latent heat transfer occurs during phase changes of water (evaporation, condensation, sublimation)
Evaporation from Earth's surface absorbs energy, while condensation in the atmosphere releases energy
Greenhouse effect is the process by which atmospheric gases (primarily water vapor and carbon dioxide) absorb and re-emit longwave radiation, warming Earth's surface
Earth's energy balance is maintained by the equilibrium between incoming solar radiation and outgoing longwave radiation
Applications in Weather Forecasting
Thermodynamic principles are crucial for understanding and predicting weather phenomena
Atmospheric stability assessment helps predict the likelihood of convection, thunderstorm development, and severe weather
Skew-T log-P diagrams are used to analyze vertical profiles of temperature, dew point, and wind, aiding in stability assessment and convection forecasting
Numerical weather prediction (NWP) models incorporate thermodynamic equations to simulate atmospheric processes and predict future weather conditions
Moisture and heat budgets are analyzed to understand energy transfer and phase changes in the atmosphere, influencing precipitation forecasts
Thermodynamic indices (e.g., CAPE, LI) are used to assess the potential for severe weather, such as thunderstorms and tornadoes
Understanding of adiabatic processes and lapse rates helps predict cloud formation, precipitation type, and the evolution of air masses
Knowledge of atmospheric composition and structure is essential for modeling radiative transfer and the greenhouse effect, which impact long-term climate forecasts