Earth receives uneven sunlight.
Latitude, season and orbital geometry create spatial and temporal contrasts.
Side 108
Climate Science
A study of the physical system that sets long-term weather statistics. Climate science links planetary energy balance, atmospheric and ocean circulation, carbon exchange, feedbacks and observations across timescales.
energy→circulation→feedback→observation→attribution
06study lenses
36working concepts
V0working model
108Side
Climate begins with the balance between incoming and outgoing energy.
Anything that changes absorbed sunlight or emitted infrared radiation can alter temperature.
Some radiation is reflected.
Clouds, ice, land and aerosols change the fraction of sunlight retained.
Earth loses energy as thermal radiation.
Warmer surfaces emit more, creating a stabilizing response.
Atmospheric gases absorb and emit infrared.
Changing concentration shifts the altitude and temperature from which energy escapes to space.
External changes perturb the balance.
Greenhouse gases, aerosols, solar changes and volcanoes create different forcing patterns.
Temperature adjusts until energy balances again.
The size and timing of adjustment depend on feedbacks and heat storage.
The climate system moves heat, water and momentum around the planet.
Atmosphere and ocean redistribute the unequal solar heating of Earth.
Tropical heating drives overturning.
Rising and sinking air help organize rainfall belts and subtropical dry zones.
Strong winds form along temperature gradients.
Their position influences storm tracks and weather persistence.
Wind and rotation organize surface currents.
Currents transport heat and shape regional climates.
Density differences connect ocean depths.
Slow circulation stores and transports heat and carbon over long timescales.
Water links energy and circulation.
Evaporation, condensation and precipitation move both moisture and latent heat.
Ocean and atmosphere interact.
Modes such as ENSO emerge from feedback between sea-surface conditions and winds.
Feedbacks amplify or damp the initial response to forcing.
The sign and strength of feedbacks determine climate sensitivity.
Warmer air holds more moisture.
Because water vapor is a greenhouse gas, warming can amplify warming.
Melting bright surfaces exposes darker ones.
Lower reflectivity increases absorbed solar energy.
Cloud responses can warm or cool.
Changes in altitude, type and coverage affect both sunlight and infrared radiation.
Warming varies with altitude.
Vertical temperature structure alters outgoing radiation.
Warming can change natural carbon uptake.
Land and ocean sinks respond to temperature, moisture and chemistry.
Warmer Earth emits more infrared.
This fundamental negative feedback stabilizes the climate system.
Climate varies naturally even without a new external forcing.
Internal variability redistributes energy and can temporarily amplify or mask longer trends.
Tropical Pacific coupling shifts globally.
El Niño and La Niña reorganize rainfall, temperature and circulation.
Large eruptions cool temporarily.
Stratospheric aerosols reflect sunlight for several years.
Solar output changes slightly.
Its observed modern contribution is smaller than major anthropogenic forcing.
Heat moves between surface and depth.
This alters the pace of surface warming without eliminating planetary energy imbalance.
Short periods remain noisy.
A cold season or record hot day alone does not establish a climate trend.
Climate emerges statistically.
Long records and spatial patterns separate persistent change from variability.
Attribution asks why an observed climate change occurred.
The strongest inference combines physical fingerprints, observations and model experiments.
Different causes leave different patterns.
Vertical, geographic and spectral responses help distinguish forcing mechanisms.
Compare worlds with and without a forcing.
Model ensembles estimate how observed outcomes change under alternative causal histories.
Track the imbalance directly.
Ocean heat content provides a major record of accumulated excess energy.
Past climates test system response.
Ice cores, sediments and other proxies extend evidence beyond instruments.
Independent observations should agree.
Temperature, ice, sea level and ocean heat constrain one another.
Ranges are part of the result.
Attribution expresses confidence and probability rather than pretending all parameters are exact.
Climate projections are conditional statements about future forcing and system response.
Scenario uncertainty, model uncertainty and internal variability dominate at different horizons and scales.
Future emissions are not a physical constant.
Socioeconomic pathways define alternative forcing trajectories.
Different models represent unresolved processes differently.
Ensembles expose structural spread rather than one deterministic forecast.
Local outcomes are harder than global means.
Topography, circulation and extremes increase uncertainty at small scales.
Distribution tails matter.
A modest shift in average temperature can strongly change the frequency of rare heat events.
Reduce harm from expected impacts.
Infrastructure, planning and behavior can lower vulnerability without changing the forcing.
Reduce the forcing itself.
Emissions cuts and carbon removal act on the cause rather than only the consequences.