Energy flows · from forcing to compartments
Surplus distribution (table)
| Compartment | Share (%) | Flux (ZJ/yr) |
|---|---|---|
| Ocean | 91 % | 11.7 ZJ/yr |
| Ice & land | 8 % | 1.0 ZJ/yr |
| Atmosphere | 1 % | 0.1 ZJ/yr |
The atmospheric share (1%) is enough to warm the air by over 1 °C; the ocean (91%) sequesters 11.7 ZJ/yr.
Ocean mechanisms
Ocean mechanisms (summary)
| Mechanism | Summary |
|---|---|
| Surplus routing | About 91% of radiative imbalance is stored in the ocean — not in the atmosphere where we live. |
| Stratification & pycnocline | The surface warms faster than the depths — the warm layer floats and slows mixing. |
| Thermosteric expansion | Warm water occupies more volume — major contribution to sea-level rise. |
| Vertical mixing | Eddies and currents spread heat — but transport slows as stratification increases. |
| Ocean inertia | The ocean takes decades to respond — hence the lag between air and depths. |
About 91% of radiative imbalance is stored in the ocean — not in the atmosphere where we live.
Water has four times the heat capacity of air and the ocean covers 71% of the surface. The atmosphere retains only ~1% of the surplus (AR6), yet that is enough to warm the air by over 1 °C since pre-industrial times.
Thermal penetration by depth
Thermal penetration by stratum (table)
| Layer | Depth | Heat share (%) | Relative intensity |
|---|---|---|---|
| Epipelagic | 0 – 300 m | 40 % | 96 % |
| Mesopelagic | 300 – 700 m | 23 % | 95 % |
| Bathypelagic | 700 – 2 000 m | 29 % | 93 % |
| Abyssal | > 2 000 m | 8 % | 91 % |
0 – 300 m
Epipelagic
40 %
300 – 700 m
Mesopelagic
23 %
700 – 2 000 m
Bathypelagic
29 %
> 2 000 m
Abyssal
8 %