Oxygen 18/16 variability in Greenland snow and ice with 10 −3 ‐ to 10 5 ‐year time resolution

The 3‐km‐long Greenland Ice Sheet Project 2 (GISP2) ice core presents a 100,000 + ‐year detailed oxygen isotope profile covering almost a full glacial‐interglacial cycle. Measurements of isotopic fluctuations in snow, frost, and atmospheric water vapor samples collected during summer field seasons (up to 20‰) are compatible with the large and abrupt 18 O/ 16 O changes observed in accumulated firn. Snow pit δ 18 O profiles from the GISP2 summit area, however, show rapid smoothing of the 18 O/ 16 O signal near the surface. Beyond about 2‐m depth the smoothed δ 18 O signal is fairly well preserved and can be interpreted in terms of average local weather conditions and climate. The longer climate fluctuations also have regional and often global significance. In the older part of the record, corresponding to marine isotope stages (MIS) 5a to 5d, the effect of orbital climate forcing via the 19‐ and 23‐kyr precession cycles and the 41‐kyr obliquity cycle is obvious. From the end of MIS 5a, at about 75,000 years B.P., till the end of the glacial at the Younger Dryas‐Preboreal transition, at 11,650 years B.P., the 18 O/ 16 O record shows frequent, rapid switches between intermediate interstadial and low stadial values. Fourier spectra of the oscillations that are superimposed on the orbitally induced changes contain a strong periodicity at 1.5 kyr, a broad peak at 4.0 kyr, and additional shorter periods. Detailed comparison of the GISP2 18 O/ 16 O record with the Vostok, Antarctica, δD record; Pacific Ocean foraminiferal 18 O/ 16 O; Grande Pile, France, tree pollen; and insolation indicates that a counterpart to many of the rapid 18 O/ 16 O fluctuations of GISP2 can be found in the other records, and that the GISP2 isotopic changes clearly are the local expression of climate changes of worldwide extent. Correlation of events on the independent GISP2 and SPECMAP time scales for the interval 10,000–50,000 years B.P. shows excellent Chronometric agreement, except possibly for the event labeled 3.1. The glacial to interglacial transition evidently started simultaneously in the Arctic and the Antarctic, but its development and its expression in Greenland isotopes was later suppressed by the influence of meltwater, especially from the Barents Sea ice sheet, on deep water formation and ocean circulation. Meltwaters from different ice sheets bordering the North Atlantic also influenced ocean circulation during the Bølling‐Allerød interstadial complex and the Younger Dryas and led to a distinct development of European climate and Greenland 18 O/ 16 O values. The Holocene interval with long‐term stable mean isotopic values contains several fluctuations with periods from years to millennia. Dominant is a 6.3‐year oscillation with amplitude up to 3 to 4‰. Periodicities of 11 and 210 years, also found in the solar‐modulated records of the cosmogenic isotopes 10 Be and 14 C, suggest solar processes as the cause of these cycles. Depression of 18 O/ 16 O values (cooling) by volcanic eruptions is observed in stacked GISP2 δ 18 O records, but the effect is small and not likely to trigger major climate changes.