Yes, ice has a high albedo compared to most surfaces on Earth, though its exact reflectivity varies widely depending on the type and condition of the ice. Fresh snow topping a glacier reflects 80 to 90 percent of incoming sunlight, while bare sea ice reflects roughly 50 to 70 percent. Even at the low end, ice is far more reflective than open ocean (which reflects only about 6 percent) or bare soil (around 17 percent). For context, Earth’s overall average albedo is about 0.30, meaning the planet reflects 30 percent of the sunlight that hits it. Most forms of ice sit well above that average.
Albedo Values for Different Types of Ice
Albedo is measured on a scale from 0 (absorbs all light) to 1 (reflects all light). Where a given piece of ice falls on that scale depends on what it looks like, how old it is, and whether snow is sitting on top of it.
Fresh, dry snow is the most reflective natural surface on Earth, with albedo values between 0.80 and 0.90. NASA estimates that if the entire planet were covered in ice, Earth’s albedo would jump to about 0.84, reflecting the vast majority of solar energy back into space. Compare that to a hypothetical Earth blanketed in dark green forest, which would have an albedo of just 0.14.
Sea ice with a snow cover ranges from about 0.50 to 0.70. Bare ice without snow is less reflective, with measurements spanning 0.10 to 0.58 depending on the ice type. On freshwater lakes, researchers have measured average ice albedo at 0.38, roughly half the reflectivity of the fresh snowfall that preceded it. Melting snow drops below 0.50 as the surface becomes wetter and grainier.
Why Fresh Ice Reflects More Than Old Ice
The main driver of ice’s reflectivity is the tiny air bubbles and ice crystals near its surface. Fresh snow contains enormous numbers of small, irregular crystals that scatter sunlight in all directions, bouncing most of it back before it can be absorbed. As snow ages, those crystals merge into larger grains, reducing the number of scattering surfaces and letting more light penetrate deeper into the snowpack.
The same principle applies to glacial ice. Blue ice areas on Antarctic ice shelves, where wind and sublimation have stripped away the surface snow layer, have albedo values of 0.50 to 0.70. That’s noticeably lower than snow-covered ice because the dense, compressed ice contains fewer air bubbles. With fewer bubbles to scatter light, shortwave radiation penetrates deeper into the ice, warming it from within.
First-Year Ice vs. Multi-Year Ice
In the Arctic, ice that has survived at least one full melt season (multi-year ice) behaves differently from ice that formed during the current winter (first-year or seasonal ice). Before melting begins, both types are snow-covered and reflect light equally. Once spring arrives, however, their paths diverge.
First-year ice has a thinner snow cover, so it transitions to bare ice faster. That bare ice also contains far fewer air bubbles in its upper layers, scatters light less effectively, and sits lower in the water. The result: first-year ice has an albedo roughly 0.1 lower than multi-year ice at the same stage (about 0.55 versus 0.65). As melting progresses, melt ponds form on both types, but first-year ice is flatter and less deformed, so meltwater spreads out in shallow ponds that can cover more than 70 percent of the surface. Multi-year ice, with its ridges and undulating topography, typically limits pond coverage to 30 to 40 percent. Since melt ponds are darker than surrounding ice, this difference drives first-year ice albedo even lower, allowing it to absorb substantially more solar energy.
The Ice-Albedo Feedback Loop
Ice’s high reflectivity is more than a curiosity. It plays a central role in regulating Earth’s temperature through a process called ice-albedo feedback. The loop works like this: when temperatures rise, ice and snow melt, exposing darker surfaces like ocean water or soil beneath. Those darker surfaces absorb more sunlight, which raises local temperatures further, which melts more ice, which exposes more dark surface. Each step reinforces the next.
The feedback works in the cooling direction too. If temperatures drop, more ice forms, reflecting more sunlight and cooling the surface further. This is why scientists describe it as a “positive feedback,” not because it’s beneficial, but because any initial change gets amplified. The mechanism has been a major factor in past ice ages and is now accelerating warming in the Arctic, where summer sea ice has declined dramatically over recent decades.
How Soot and Pollution Lower Ice Reflectivity
Ice doesn’t need to melt to lose its reflectivity. Black carbon, the dark particulate matter produced by burning fossil fuels and biomass, settles on snow and ice surfaces and dramatically reduces their ability to reflect sunlight. Even small amounts make a visible difference. Estimates suggest that soot reduces albedo by about 1.5 percent in the Arctic and 3 percent across Northern Hemisphere land areas, which translates to an additional warming effect of roughly 0.3 watts per square meter across the Northern Hemisphere.
Laboratory and field studies have found that black carbon particles are two to five times more effective at reducing snow albedo than early theoretical models predicted. The particles don’t just sit on the surface. When embedded inside ice crystals rather than resting on top, their light-absorbing power increases by 40 percent or more. Particle shape matters too: needle-shaped or flat soot particles absorb more light per unit of mass than spherical ones.
This contamination has contributed to earlier spring snowmelt, thinning Arctic sea ice, and accelerating the loss of glaciers and permafrost. Reducing soot emissions would help restore snow and ice albedo closer to its naturally high values, slowing the feedback loop that is amplifying warming in ice-covered regions.