Category: Poster

Ice shelves are thick floating platforms of ice that connect land and ocean. Since 2016, sustained warming has led to significant and increasing Antarctic basal melting - melting of the underside of ice an shelf by the ocean. The rate of basal melting is primarily influenced by the characteristics of the sub-ice shelf–ocean boundary layer, a turbulent region responsible for the exchange of heat and salt between the ocean and the ice. This turbulent layer is usually driven by convection or shear-driven processes. As ice shelves thin due to basal melting, their ability to support the ice upstream decreases, leading to an increase in the ice flow from land to sea and subsequent sea level rise. Most of the heat responsible for melting ice shelves is transported by ocean currents flowing into the cavities beneath the ice shelves. Recent observations from ApRES (Autonomous phase-sensitive Radio-Echo Sounder) at the Fimbul Ice Shelf in East Antarctica have detected a long-term mean ablation rate of up to 1.0 ± 0.4 meters per year beneath the central region of the ice shelf. Further observations from 2017 to 2021 have shown sub-weekly to monthly variations in basal melting rates attributed to shear-driven turbulent heat transfer processes along with seasonal variations driven by ocean warming during the austral summer.

Due to increasing temperatures, the sea ice is thinning and weakening in the Arctic. This makes sea ice more prone to changes from atmospheric forcings such as wind and waves. In the Marginal Ice Zone (MIZ) there are many processes occurring, and one of them are waves-in-ice dynamics. Researchers are trying to implement these processes in coupled ice-ocean models, but due to large differences in types of ice and ice thickness it is hard to find a good model accounting for every physical process.
The poster will review how ice thickness and floe size influences waves when the waves are dampened by the ice. It is hard to directly measure the specific influence of ice thickness and floe size in the MIZ due to the large differences in ice characteristics over small areas, difficult access and rapid changes. Therefore most data are collected in land-fast ice, however some research has been done directly in the MIZ based upon visual estimates. It is clear that increasing ice thickness and floe size attenuate and dampen waves to a greater extent than thinner ice. This could have impacts on the Arctic ecosystems, specifically due to an increasing MIZ when the sea ice is thinner, so waves can travel further and open areas which have been closed and protected by sea ice.

The density of water depends on temperature, salinity and pressure. When sea ice forms brine rejection takes place which leads to an increase in the density of the underlying water. Depending on the ocean stratification, this can lead to convection where the denser water sinks. This type of convection is called type I convection and occurs regularly during winter in polar seas. It slowly deepens the mixed layer as the pycnocline gets eroded. However, there is also a type II convection that can only take place under specific circumstances, and which can lead to ventilation of the entire water column. This type of convection relies on thermobaricity: the effect of pressure on water’s density. Colder, fresh waters get more compressed (and thus dense) under pressure than warm, saline waters. This means that a seemingly stable ocean profile might be unstable when a water parcel reaches a depth where thermobaricity becomes important. This can then result in type II convection. However, in order to get a type II convection, the background stratification needs to be overcome. The normalised strength of thermobaricity indicates the likeliness of this to happen. Still, there is another important factor that determines whether type II convection can occur: the thermobaric barrier. This poster dives into the processes controlling thermobaricity and examines a case study over Maud Rise near Antarctica. Lastly, it provides an overview of stratification types in the World oceans.

Convection and deep-water formation in the Greenland Sea play crucial roles in the Atlantic Meridional Overturning Circulation (AMOC). Much of this convection occurs along the sea-ice edge, driven by strong temperature gradients between the atmosphere and the exposed ocean. This process leads to cooling of the surface layer, resulting in increased density and subsequent sinking of surface waters. As the climate changes, due to global warming, the sea-ice edge is retreating, causing a re-organization of water mass transformation. Understanding this re-organization is essential, as the AMOC significantly impacts global climate and temperatures, as well as regional climate here in Bergen. This poster investigates the relationship between sea-ice edge retreat and convection in the Greenland Sea. It highlights a significant retreat of the sea-ice edge along the east coast of Greenland over recent decades, particularly noticeable during the winter months when convection is most active. Additionally, the poster explores how the re-organization of convection could imply both a weakening or even give resilience to the AMOC. By examining these dynamics, the poster shed light on relationships between the sea-ice edge, convection, and broader implications for global climate.

Polynyas are primarily open water sea ice free areas surrounded by sea ice, formed by either strong winds or oceanic currents that drives away the sea ice. There are two types of polynyas: coastal polynyas (very thin ice present) and open water polynyas (no sea ice). For both types of polynyas, it is the direct contact between the atmosphere and the water that leads to the formation of deep water. Indeed, the water will cool much faster in polynyas thanks to the absence of sea ice or the presence of very thin sea ice, thus the water will be denser and even more so with the salinity released from the surrounding sea ice. The two main areas for deep water production are the North Atlantic (North Atlantic Deep Water (NADW)) and the Southern Ocean (Antarctic Bottom Water (AADW)).