In 1978, a small island was discovered north of Kaffeklubben Ø, until then considered the most northern island on Earth. This island was named Oodaaq Ø. It was visited again in 1979, and in 1980 it was seen from Kaffeklubben Ø by members of the Sirius sledge patrol. Sirius searched for Oodaaq Ø again from 1981 to 1984 but did not find it. During the period from 1996 to 2008, the region was visited regularly and a number of new islets were discovered: the 1996 ATOW Island, KMS Island, 2001 RTOW Island, 83-42 Island, Stray Dog West Island and the 2008 Island. The islets are composed of gravel. We believe the area with islets is shallow, being a continuation of a coastal plain to the south. We suggest that the sea floor in the area is irregular and that the islets form by floes of sea ice that bulldoze material from the sea floor up above sea level. In some cases, perhaps all, the islets disappear when sea ice floes bulldoze sediment back below sea level. Alternatively, the so-called islets are just accumulations of gravel on sea ice.

The subantarctic island of South Georgia provides terrestrial and coastal marine records of climate variability, which are crucial for the understanding of the drivers of Holocene climate changes in the subantarctic region. Here we investigate a sediment core (Co1305) from a coastal inlet on South Georgia using elemental, lipid biomarker, diatom, and stable isotope data to infer changes in environmental conditions and to constrain the timing of late-glacial and Holocene glacier fluctuations. Because of the scarcity of terrestrial macrofossils and the presence of redeposited and relict organic matter in the sediments, age control for the record was obtained by compound-specific radiocarbon dating of mostly marine-derived n-C16 fatty acids. A basal till layer recovered in Little Jason Lagoon was likely deposited during an advance of local glaciers during the Antarctic cold reversal. After glacier retreat, an oligotrophic lake occupied the site, which transitioned to a marine inlet around 8.0±0.9 ka because of relative sea-level rise. From 7.0±0.6 to 4.0±0.4 ka, reduced vegetation coverage in the catchment, as well as high siliciclastic input and deposition of ice-rafted debris, indicates glacier advances in the terrestrial catchment and likely in the adjacent fjord. A second, less extensive period of glacier advances occurred in the late Holocene, after 1.8±0.3 ka.

A lacustrine sediment record from the Kangerlussuaq region, West Greenland, has resulted in a pollen, macrofossil, and sediment stratigraphy that encompasses the last 5000 14C yr. Deglaciation of the area and subsequent development of a nearby floodplain occurred before 5000 yr B.P. Since that time eolian sand and silt deposition appear to have been continuous, with a significant increase ca. 1000 14C yr B.P. Pollen analysis shows little change in the character of the vegetation throughout the record. Fluctuations in herb pollen taxa indicate changes in the extent and development of eolian sand sheets. The oldest pollen zone records relatively little pollen accumulation and low taxa diversity. This is followed by a zone of high pollen accumulation, presumably a phase of highest vegetation density, from 4400 to 3400 14C yr B.P. Thereafter, declining pollen accumulation rates reveal a gradual environmental deterioration. Macrofossil analyses record significant limnological changes, with an early eutrophic phase followed by a masotrophic phase and a reversal to more eutrophic conditions in the final phase. The preserved record illustrates the interactions of deglaciation, eolian activity, regional vegetation, and limnological change.

Radiocarbon age determination of a Greenland whale (Balaena mysticetus) vertebra from Melville Bugt in northwestern Greenland yields an age of 9259–8989 cal yr BP. The margin of the Greenland Ice Sheet in Melville Bugt was situated behind its AD 1950–2000 position in the early Holocene, at a similar position to that being reached following rapid retreat in recent years. Such an early deglaciation of areas close to the Greenland Ice Sheet is unusual. This probably reflects the unique glaciological setting resulting from the narrow fringe of ice-free islands and peninsulas and offshore waters with deep areas that characterize this part of Greenland. The timing of Greenland Ice Sheet retreat to its present margin varies significantly around Greenland.

The presence of glacial sediments across the Rauer Group indicates that the East Antarctic ice sheet formerly covered the entire archipelago and has since retreated at least 15 km from its maximum extent. The degree of weathering of these glacial sediments suggests that ice retreat from this maximum position occurred sometime during the latter half of the last glacial cycle. Following this phase of retreat, the ice sheet margin has not expanded more than ∼ 1 km seaward of its present position. This pattern of ice sheet change matches that recorded in Vestfold Hills, providing further evidence that the diminutive Marine Isotope Stage 2 ice sheet advance in the nearby Larsemann Hills may have been influenced by local factors rather than a regional ice-sheet response to climate and sea-level change.

High-resolution lithostratigraphy, mineral magnetic, carbon, pollen, and macrofossil analyses, and accelerator mass spectrometry 14C measurements were performed in the study of a sediment sequence from Lake Tambichozero, southeastern Russian Karelia, to reconstruct late-glacial and early Holocene aquatic and terrestrial environmental changes. The lake formed ca. 14,000 cal yr B.P. and the area around the lake was subsequently colonized by arctic plants, forming patches of pioneer communities surrounded by areas of exposed soil. A minor rise in lake productivity and the immigration of Betula pubescens occurred ca. 11,500 cal yr B.P. The rise in summer temperatures probably led to increased melting of remnant ice and enhanced erosion. The distinct increase in lake productivity and the development of open Betula-Populus forests, which are reconstructed based on plant macrofossil remains, indicate stable soils from 10,600 cal yr B.P. onward. Pinus and Picea probably became established ca. 9900 cal yr B.P.

We constrain the history of the Greenland Ice Sheet margin during the Holocene at Upernavik Isstrøm, a major ice stream in northwestern Greenland. Radiocarbon-dated sediment sequences from proglacial-threshold lakes adjacent to the present ice margin constrain deglaciation of the sites to older than 9.6 ± 0.1 ka. This age of deglaciation is confirmed with 10Be ages of 9.9 ± 0.1 ka from an island adjacent to the historical ice position. The lake sediment sequences also constrain the ice margin to have been less extensive than it is today for the remainder of the Holocene until ~ 1100 to ~ 700 yr ago, when it advanced into two lake catchments. The ice margin retreated back out of these lake catchments in the last decade. The early Holocene deglaciation in Melville Bugt, one of few locations around Greenland where a vast stretch of the current ice margin is marine-based, preceded deglaciation in most other parts of Greenland. Earlier deglaciation in this ice-sheet sector may have been caused by additional ablation mechanisms that apply to marine-based ice margins. Furthermore, despite ice-sheet models depicting this sector of Greenland as relatively stable throughout the Holocene, our data indicate a > 20 km advance-retreat cycle within the last millennium.

The Thule region in north Greenland formerly supported a population of musk-oxen (Ovibos moschatus). Radiocarbon dating of bones of this mammal collected on the terrain surface and from archaeological sites has yielded late Holocene ages, indicating that the species was a late immigrant to this part of Greenland. The species may have arrived at a time when the area was uninhabited, and it had at least a thousand years to spread south, before the Late Dorset people arrived. The heavy glaciation of Melville Bugt in the late Holocene was probably the main reason that the musk-ox did not disperse south to west Greenland. The population of musk-ox in the region may have peaked during the Medieval Warm Period, and the species survived during the occupation of the region by the Late Dorset people. The size of the population may have declined during the beginning of the Little Ice Age, and musk-ox was probably exterminated from the region shortly after the arrival of the mobile Thule people.

Radiocarbon age determinations on shells of the common mussel (Mytilus edulis) show that this species was present in central East Greenland from approximately 9500 to 5400 cal. years BP. It probably arrived first at the outer coast, at a time when the inner parts of the fjords were still occupied by glaciers. After perhaps a millennium it spread to the central fjord region where it lived for at least three millennia. The former occurrence of Mytilus edulis indicates higher sea surface temperatures than at present and more extensive fjord water, which may have been a consequence of higher summer insolation, perhaps amplified by changes in atmospheric circulation, bringing more warm air masses to the north. The timing of the Holocene thermal maximum in the lowlands of East Greenland was later than recorded in the Renland ice core. This delay was probably related to the continuing recession of the margin of the Greenland ice sheet in the early Holocene. The lingering decaying ice meant that large lowland areas were still ice covered, and other areas were cooled by the ice.

Germania Havn Sø is located at the outermost coast of northeastern Greenland. According to radiocarbon dating, the lake basin was deglaciated in the early Holocene, around 11,000 cal yr BP. At that time the lake was a marine bay, but the lake was isolated soon after deglaciation at ~ 10,600 cal yr BP. The marine fauna was species-poor, indicating harsh conditions with a high sedimentation rate and lowered salinity due to glacial meltwater supply. The pioneer vegetation around the lake was dominated by mosses and herbs. Deposition of relatively coarse sediments during the early Holocene indicates erosion of the newly deglaciated terrain. Remains of the first woody plant (Salix herbacea) appear at 7600 cal yr BP and remains of other woody plants (Salix arctica, Dryas octopetala, Cassiope tetragona and Empetrum nigrum) appear around one millennium later. Declining concentrations of D. octopetala and the caddis fly Apatania zonella in the late Holocene probably imply falling summer temperatures. Only moderate changes in the granulometric and geochemical record during the Holocene indicate relatively stable environmental settings in the lake, which can probably be explained by its location at the outer coast and the buffering effect of the neighboring ocean.

In the light of data from the Greenland ice sheet concerning the ice-age climate, and palaeoecological studies of interglacial and Early Holocene deposits, the concept that a large proportion of Greenland's plants and animals may have survived during the ice ages is evaluated. While ice-free areas (refugias) were present, it is concluded that only hardy, cold-adapted species could have survived, which also explains why so few clearly endemic species are present in Greenland. Most members of the present biota are considered to be postglacial immigrants. Some species came to Greenland by walking or flying, but most arrived by passive, long-distance, chance dispersal, carried by wind, sea currents, and, in particular, birds. Transport by birds may explain why so many species arrived from Europe, because vast numbers of geese in particular migrate from northwest Europe to Greenland.

The evolution of the East Antarctic Ice Sheet (EAIS) during the Late Quaternary is poorly known, partly because some regions, such as the Prydz Bay vicinity, indicate significant variability in the glaciation patterns (e.g. Domack et al. 1998, Zwartz et al. 1998, Hodgson et al. 2005).

Radiocarbon age determinations of 32 walrus (Odobenus rosmarus) remains show that the species has been a member of the Greenland fauna since at least the middle Holocene. The oldest date is 7280–7160 calendar years BP. However, most dated remains come from archaeological sites and are of late Holocene age

The small island of Tuppiap Qeqertaa, formerly known as Tobias Ø or Tobias Island, is situated 80 km off the northeast Greenland coast. The island was discovered in 1993 and is approximately 2 km long and 1.5 km wide. Most of the island is covered by an ice cap that rises to 35 m above sea level, as determined by airborne laser scanning. High-quality geodetic GPS measurements determine the position of a small cairn erected on the island to 79°20′34.48′′ N, 15°46′31.23′′ W. Minor parts of the island are ice free, with small hills of gravel. Late Holocene shells of marine bivalves have been found and were presumably brought up by ice floe push. Shell fragments of southern extralimital marine invertebrates point to the presence of pre-Holocene deposits. Three species of moss are the only land plants that have been found on the island.

Northeast Greenland supports a large indigenous population of musk-oxen (Ovibosmoschatus). Radiocarbon dating of remains of this mammal collected on the terrain surface and from archaeological sites has yielded mid- and Late Holocene ages. The species probably arrived shortly before this part of Greenland became inhabited by the first hunter cultures. Only Late Holocene dates are available from the southern part of northeast Greenland, but the authors suggest that musk-ox spread south to this region at an early date, because there are no physical barriers. The lack of older dates may reflect the lack of palaeo-Eskimo sites with bones.

Northwest Greenland formerly supported a population of musk-ox (Ovibos moschatus). Radiocarbon dating of musk-ox remains collected on the terrain surface and from archaeological sites has yielded Late Holocene ages, indicating that the species was a late immigrant to this part of Greenland. Musk-ox arrived at a time when Greenland was uninhabited, and the species had at least several hundred years to expand and spread south, before the Late Dorset people arrived and began to hunt. The main reason that the species did not disperse south to West Greenland was probably because of the barrier presented by Melville Bugt, which was heavily glaciated in the Late Holocene. However, if there had been a longer period of time before hunting of the musk-ox occurred, there would have been an enhanced likelihood that chance dispersal south could have taken place.