Meteorology

☁️Meteorology Unit 3 – Solar Radiation and Earth's Energy Balance

Solar radiation powers Earth's climate system, driving atmospheric and oceanic circulation. This unit explores how the Sun's energy interacts with our planet, from its journey through space to its absorption, reflection, and re-emission by Earth's surface and atmosphere. Understanding Earth's energy balance is crucial for grasping climate dynamics. We'll examine concepts like albedo, the greenhouse effect, and feedback loops, as well as how scientists measure and model solar radiation to predict climate patterns and changes.

Key Concepts and Terminology

  • Solar radiation the primary source of energy for Earth's climate system
  • Electromagnetic spectrum range of all possible frequencies of electromagnetic radiation
    • Includes radio waves, microwaves, infrared, visible light, ultraviolet, X-rays, and gamma rays
  • Insolation amount of solar radiation received on a given surface area during a specific time interval
  • Albedo fraction of solar radiation reflected by a surface or object
    • Ranges from 0 (completely black) to 1 (completely reflective)
  • Greenhouse effect process by which atmospheric gases trap heat radiating from Earth's surface
  • Blackbody an idealized physical object that absorbs all incident electromagnetic radiation
  • Stefan-Boltzmann law states that the total energy radiated per unit surface area of a blackbody is directly proportional to the fourth power of its absolute temperature

The Sun as Earth's Energy Source

  • Sun is the central star of our solar system and the primary energy source for Earth
  • Powered by nuclear fusion reactions in its core, converting hydrogen into helium
  • Emits electromagnetic radiation across a wide spectrum, with peak emission in the visible light range
  • Solar energy drives Earth's climate system, including atmospheric and oceanic circulation patterns
  • Variations in solar output can influence Earth's climate over long timescales
    • Examples include the 11-year solar cycle and longer-term changes in solar activity
  • Distance between Earth and the Sun (1 astronomical unit or AU) affects the amount of solar radiation received
  • Earth's axial tilt and orbital eccentricity contribute to seasonal variations in solar insolation

Solar Radiation Basics

  • Solar radiation consists of electromagnetic waves emitted by the Sun
  • Intensity of solar radiation decreases with distance from the Sun following an inverse square law
  • Solar radiation spectrum spans from short-wavelength gamma rays to long-wavelength radio waves
    • Visible light makes up a small portion of this spectrum
  • Peak wavelength of solar emission is around 500 nanometers (green light)
  • Solar constant average amount of solar radiation received at the top of Earth's atmosphere (approximately 1,360 W/m²)
  • Atmospheric gases, aerosols, and clouds can absorb, scatter, or reflect incoming solar radiation
  • Shorter wavelengths (ultraviolet) are more easily scattered by atmospheric particles (Rayleigh scattering)
    • This is why the sky appears blue

Earth's Energy Budget

  • Earth's energy budget balance between incoming solar radiation and outgoing terrestrial radiation
  • Incoming solar radiation (insolation) is mostly in the visible and near-infrared wavelengths
  • Approximately 30% of incoming solar radiation is reflected back to space by clouds, aerosols, and Earth's surface
  • Remaining 70% is absorbed by the atmosphere, oceans, and land surfaces
  • Earth emits longwave (infrared) radiation back to space to maintain energy balance
  • Greenhouse gases (water vapor, carbon dioxide, methane) absorb and re-emit some of this outgoing infrared radiation
    • This process warms the lower atmosphere and surface
  • Global energy balance determines Earth's average temperature and climate patterns

Atmospheric Interactions with Solar Radiation

  • Earth's atmosphere interacts with incoming solar radiation through absorption, scattering, and reflection
  • Atmospheric gases absorb specific wavelengths of solar radiation
    • Ozone absorbs harmful ultraviolet radiation in the stratosphere
    • Water vapor and carbon dioxide absorb infrared radiation
  • Scattering of solar radiation by atmospheric particles (aerosols) and molecules affects the amount reaching the surface
    • Rayleigh scattering by air molecules is more effective at shorter (blue) wavelengths
    • Mie scattering by larger particles (dust, pollutants) is less wavelength-dependent
  • Clouds play a significant role in reflecting solar radiation back to space (cloud albedo)
    • Low, thick clouds (stratus) have a higher albedo than high, thin clouds (cirrus)
  • Atmospheric absorption and scattering can lead to diffuse solar radiation (skylight) in addition to direct sunlight

Albedo and Surface Effects

  • Albedo the fraction of incoming solar radiation reflected by a surface
  • Different surfaces have varying albedos, affecting the amount of solar energy absorbed
    • Fresh snow has a high albedo (0.8-0.9), while dark forests have a low albedo (0.1-0.2)
  • Changes in land cover (deforestation, urbanization) can alter surface albedo and impact local climate
  • Ocean albedo varies with surface conditions and sun angle
    • Calm, smooth water has a lower albedo than choppy, rough seas
  • Ice-albedo feedback a positive feedback mechanism where melting ice reduces surface albedo, leading to increased absorption of solar radiation and further warming
  • Urban heat island effect cities tend to have lower albedos and higher temperatures compared to surrounding rural areas
    • Due to dark surfaces (asphalt, rooftops) and reduced vegetation

Climate Implications and Feedback Loops

  • Changes in Earth's energy budget can have significant impacts on global climate
  • Positive feedback loops amplify initial changes, while negative feedback loops dampen them
  • Examples of climate feedback loops related to solar radiation:
    • Ice-albedo feedback (positive): Melting ice reduces surface albedo, leading to more absorption of solar radiation and further warming
    • Water vapor feedback (positive): Warmer air can hold more water vapor, a potent greenhouse gas, leading to additional warming
    • Cloud feedback (uncertain): Changes in cloud cover and properties can either amplify or dampen warming, depending on cloud type and altitude
  • Long-term variations in Earth's orbit (Milankovitch cycles) affect the distribution of solar radiation and contribute to glacial-interglacial cycles
  • Anthropogenic activities (greenhouse gas emissions, land-use changes) can alter Earth's energy balance and drive climate change

Measuring and Modeling Solar Radiation

  • Accurate measurements of solar radiation are crucial for understanding Earth's energy budget and climate system
  • Instruments used to measure solar radiation:
    • Pyranometers measure global (direct + diffuse) solar radiation on a horizontal surface
    • Pyrheliometers measure direct solar radiation at normal incidence
    • Pyrgeometers measure longwave (infrared) radiation emitted by the atmosphere and surface
  • Satellite observations provide global coverage of solar radiation and Earth's energy budget
    • Examples: NASA's CERES (Clouds and the Earth's Radiant Energy System) and SORCE (Solar Radiation and Climate Experiment) missions
  • Climate models incorporate solar radiation and Earth's energy budget to simulate past, present, and future climate conditions
    • Models consider factors such as atmospheric composition, surface properties, and cloud cover
  • Comparing model simulations with observations helps improve our understanding of the climate system and the role of solar radiation


© 2024 Fiveable Inc. All rights reserved.
AP® and SAT® are trademarks registered by the College Board, which is not affiliated with, and does not endorse this website.

© 2024 Fiveable Inc. All rights reserved.
AP® and SAT® are trademarks registered by the College Board, which is not affiliated with, and does not endorse this website.