Despite global BC may have increased from 1990 to 2010, Arctic BC decreased dramatically over that same time span [19; 23; 24]. At Alert (Canada) the decrease from 1989-2003 reaches about 50% [24]. The decline of Arctic BC has been attributed to the dissolution of the Soviet Union, resulting in the closing of emission sources in Russia and Eastern Europe, and depopulation of the Russian Arctic [25]. Estimated BC deposition in the Arctic varies between 8 and more than 13 TgC yr\({}^{-1}\) and is highly dependent on aerosol size containing the BC and the mixing state [26] with dry deposition contributing up to 40% of the total removal [27]. Direct BC deposition measurements and documented behaviour in the snow pack are still limited despite previous efforts to include microphysical properties and chemistry related to aging in order to provide a successful simulation of BC concentrations deposited over the Arctic [25; 27]. In addition, the few available measurements of the dry deposition of submicron particles over snow display a large variability (0.02 to 0.33 cm s\({}^{-1}\)[28; 29]). For areas with a high ratio of dust to BC, the scavenging effect will enforce an increasingly dominance of dust over BC [30]. This is what we presume to take place in our study area. Nearby our study site, a field experiment aiming at the characterization of ice types, albedo and impurity content was conducted in 2006 [31]. The team of [PERSON] et al. [31] found, that the mineralogical composition of most impurities matches that of the surrounding soils, suggesting that most of the material is derived from local sources. If equally distributed, these impurities are found to reduce the albedo of Holocene ice to 0.2-0.4. Interestingly, ice with more impurities per unit area, but aggregated in cryoconite holes, reaches an albedo of 0.6 as the impurities are shaded by the walls of the hole. [PERSON] et al. [13] investigated a prominent dark area of the Greenland Ice Sheet by means of optical remote sensing using the MODIS sensors. They introduced a distinction between so called bare ice and dark ice using the reflectance at different wavelengths. Bare ice is defined at \(\lambda=860\) nm (band 2) with a reflectance of less than 0.6, while dark is defined at \(\lambda=660\) nm (band 1) with a reflectance of less than 0.4. [PERSON] et al. [13] find a maximum of 1.5% of the ice sheet to consist of dark ice. In the following we are referring to this classification, using Sentinel-2 bands of similar wavelength. It has also been found that wind-blown sedimentary rock particles that form a layer of debris are the dominant trigger for surface melt ponds on the George VI Ice Shelf in Antarctica [32]. The setting of George VI Ice Shelf with the nearby mountains of Alexander Land is similar to our study area at the margin of the North-East Greenland Ice Stream (NEGIS) and in particular the lower range of 79\({}^{\circ}\) Glacier (79 NG). In this study, we take advantage of changes of drainage of supraglacial lakes leaving a bright surface and measure changes in reflectance over few years and set this into the context of surface properties along a fast flowing outlet glacier and a nearby slow moving area with exposed ice age ice.