Lofoten Vortex

The Lofoten Vortex, also called Lofoten Basin Vortex or Lofoten Basin Eddy, is a permanent oceanic anticyclonic eddy, located in the northern part of the Norwegian Sea, off the coast of the Lofoten archipelago. It was documented for the first time in the 1970s. Due to the presence of the permanent vortex, the Lofoten basin features a localised area with high levels of sea surface temperature and eddy kinetic energy. The local currents inside the vortex and the strong convection observed during winter generate a hot spot rich in nutrients, affecting the surrounding marine biology. Moreover, due to its extraordinary persistence and location, the Lofoten Vortex is likely to influence the dense water formation in the region.

Physical properties

The Lofoten Basin is a well-defined topographic depression of about 3250 m depth, situated between the Norwegian continental slope in the east, the Vøring Plateau and the Helgeland Ridge in the south and southwest, and the Mohn Ridge in the northwest. The complex bathymetric structure is pivotal to locate the two major ocean currents of the basin:

the Norwegian Atlantic Slope Current (NwASC), which flows south-north all along the continental shelf of Norway; the Norwegian Atlantic Front Current (NwAFC), which streams almost parallel to the slope current, but down the west side of the Vøring Plateau and then along the Mohn Ridge. These currents play a key role in the mechanisms that guarantee the persistence of the Lofoten Vortex. The vortex has been localised in the deepest part of the Lofoten Basin. It is an apparent permanent anticyclonic eddy, whose persistence has been documented in the past years by shipborne, Seagliders and satellite measurements. The estimated radius of the vortex is 15–20 km and presents a 1200 m thick core of Atlantic Water (warm and saline) swirling at velocities that reach 0.8 m/s at 600–800 m depth. The velocity structure is similar to a Rankine vortex, characterised by a slow, outward decrease in azimuthal velocities. RAFOS floats trapped in the core of the Lofoten Vortex revealed that the vortex centre travelled 1850 km in 15 months, with an average drifting speed of 1 to 5 km/day, but with peaks reaching 15 km/day. From these measurements, a general downslope and counter-clockwise movement of the vortex around the deepest part of the Lofoten Basin is detected. From salinity and temperature profiles it is possible to see that the internal hydrography of the vortex is characterised by a doubly convex lens structure. The doming isotherms, upward at around 200 m and downward at approximately 600 m depth, are visible in a vertical mean temperature profile. This structure reveals that the deep Lofoten Basin is a major convection site in the Nordic Seas, specifically in winter: inside the Lofoten Vortex, the Atlantic Water penetrates up to 800 m depth, much deeper than in any other location of the same sea. Strong seasonality characterises the density profile of the vortex: during summer a double core structure is detectable, with a shallow pycnocline created by the stratification of surface water heated by the sun. On the other hand, in winter the surface's cooling creates strong convection that homogenises the density profile and deepens the pycnocline up to 1200 m depth.

Surface signature and tracking

The Lofoten Vortex has two surface features that are useful for its detection. First, on a sea surface temperature (SST) map, the vortex is recognisable as a negative SST anomaly. The cold-core surface signature, however, cannot be consistently detected by satellites' records, therefore it is not usually addressed as a reliable tracking method. Being an anticyclonic structure, the Lofoten Vortex can instead be analysed as a positive sea level anomaly (SLA). Satellites measuring SLA highlighted the persistent existence of the vortex in 83% of the available datasets, with a lifetime spanning from 90 days up to more than one year. The longest registered vortex lasted for two years, from May 2002 to April 2004. It is necessary to point out that in the period between two identified vortices, it is uncertain if the vortex disappeared or was simply not detected. That could be the case when the vortex adopts a submesoscale structure, with a non-detectable SLA.

Mechanisms sustaining the Lofoten Vortex Two mechanism has been identified so far, both playing an important role in the formation and the sustainment of the Lofoten Vortex:

Merging of smaller anticyclones generated by the NwASC. Wintertime convection.

Anticyclonic merging

Anticyclones' genesis region The Lofoten vortex is situated in the deepest parts of the topographic depression of the Lofoten Basin. Due to the instabilities of the basin’s eastern boundary current (NwASC), cyclones and anticyclones are shed off from the east. As shown by experiments in a rotating tank, cyclones climb upslope in an anticyclonic spiral relative to the centre of a seamount, and anticyclones will descend towards the centre of a bottom depression in a cyclonic spiral. Likewise, the anticyclones released from the Norwegian Atlantic Slope Current (NwASC) spiral counterclockwise towards the deepest part of the Lofoten Basin. Some of the anticyclones terminate within the basin, whilst the longer-lasting trajectories (of 3–6 months) are traced back to the slope region related to the elevated eddy kinetic energy. The anticyclonic source region can be divided into two areas of generation, following different paths into the basin:

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