Earth's energy storage changes when incoming and outgoing energy differ.
Key knowledge
At the top of the atmosphere, Earth's radiative balance compares incoming sunlight with reflected sunlight and outgoing thermal radiation. On a global average, sustained net energy input increases energy stored in the Earth system; radiative equilibrium requires balanced incoming and outgoing fluxes.
Conditions and scope
This is a global boundary budget, not a requirement that every place or moment be in balance.
The equilibrium description is an idealized condition, not an assertion that today's climate is in equilibrium.
Sources · 2
References
Sources retain their recorded scope. A source link alone does not establish verification of every statement.
NASA's global energy-budget definition and equilibrium distinction; no historic flux estimate is treated as current measurement.
2026-10-10 · English incoming/reflected/outgoing accounting checked against the energy-budget overview; transient and regional details are excluded.
Foundational review
2026-10-10 · Fresh primary-source inspection of the complete compact record, including every statement, equation, quantity and material condition, followed by independent AI editorial review. This check does not certify all linked lessons or every passage of every cited publication.
Sources from other places
Scope or convention differs
Absorption, reflection and emission processes contributing to the radiation budget.
This source comparison covers radiation processes; it does not independently check the full top-of-atmosphere balance equation.
The water cycle describes water storage and movement among the atmosphere, surface and subsurface. Water can be liquid, solid or gas. Solar energy and gravity drive its movement, while human activities alter storage, flow and water quality.
At the top of the atmosphere, Earth's radiative balance compares incoming sunlight with reflected sunlight and outgoing thermal radiation. On a global average, sustained net energy input increases energy stored in the Earth system; radiative equilibrium requires balanced incoming and outgoing fluxes.
Solar energy drives water movement and evaporation transfers energy within the Earth system.
Greenhouse gases absorb and emit thermal infrared radiation. This affects outgoing heat loss and allows Earth's surface and lower atmosphere to be warmer than they would be without those gases under comparable solar input.
At the top of the atmosphere, Earth's radiative balance compares incoming sunlight with reflected sunlight and outgoing thermal radiation. On a global average, sustained net energy input increases energy stored in the Earth system; radiative equilibrium requires balanced incoming and outgoing fluxes.
Greenhouse absorption and emission are components of the radiative energy budget.
Ocean circulation includes wind-driven currents and overturning associated with buoyancy changes from heating, cooling and freshwater exchange. These processes redistribute heat and materials. Deep-water formation and the return of water toward the surface involve connected dynamics rather than a single uniform conveyor speed.
Ocean circulation redistributes heat and interacts with surface heat exchange.
Unequal solar heating and Earth's rotation help organize atmospheric circulation. Tropical rising motion and subtropical descent form a broad Hadley circulation, while prevailing winds and other circulation patterns redistribute heat and moisture. Storms and regional geography modify the broad pattern.
A well-mixed layer of fixed depth H with constantρ₀,c_p and negligible lateral/entrainment heat transport has ρ₀c_pH dT/dt=Q_net,where Q_net is the total net heat input per horizontal area. Thus equal surface heating produces different rates of temperature change for different thermal inventories. If depth changes or water is exchanged, its carried heat must also be included.
For solar flux S perpendicular to the rays at the current orbital distance,latitudeφ and declinationδ give cosZ=sinφsinδ+cosφcosδcosh. Integrating positive illumination over a rotation gives meanQ=(S/π)[h₀sinφsinδ+cosφcosδsinh₀]. For ordinary sunrise/sunset h₀=arccos(−tanφtanδ); polar-day/night limits use h₀=π or0 with the appropriate geometry.
Top-of-atmosphere input and surface thermal response are distinct quantities.
A Landsat thermal-band TOA radianceL_λ>0 maps to product brightness temperature T_B=K₂/ln(K₁/L_λ+1), using its band-specific metadata constants. Brightness temperature is the equivalent blackbody temperature for the specified radiance/band convention; atmospheric effects and surface emissivity separate it from the physical temperature of the ground or sea surface.
Observed brightness is distinct from a surface heat budget.