Glacial cycles: toward a new paradigm

Abstract. The largest environmental changes in the recent geological history of the Earth are undoubtedly the successions of glacial and interglacial times. It has been clearly demonstrated that changes in the orbital parameters of our planet have a crucial role in these cycles. Nevertheless, several problems in classical astro-nomical theory of paleoclimate have indeed been iden-tified: (1) The main cyclicity in the paleoclimatic record is close to 100,000 years, but there is no significant orbitally induced changes in the radiative forcing of the Earth in this frequency range (the “100-kyr problem”); (2) the most prominent glacial-interglacial transition occurs at a time of minimal orbital variations (the “stage 11 problem); and (3) at;0.8 Ma a change from a 41-kyr dominant periodicity to a 100-kyr periodicity occurred without major changes in orbital forcing or in the Earth’s configuration (the “late Pleistocene transition prob-lem”). Additionally, the traditional view states that the climate system changes slowly and continuously together with the slow evolution of the large continental ice sheets, whereas recent high-resolution data from ice and marine sediment cores do not support such a gradual scenario. Most of the temperature rise at the last termi-nation occurred over a few decades in the Northern Hemisphere, indicating a major and abrupt reorganiza-tion of the ocean-atmosphere system. Similarly, huge iceberg discharges during glacial times, known as Hein-rich events, clearly demonstrate that ice sheet changes may also be sometimes quite abrupt. In light of these recent paleoclimatic data the Earth climate system ap-pears much more unstable and seems to jump abruptly between different quasi steady states. Using the concept of thresholds, this new paradigm can be easily integrated into classical astronomical theory and compared with recent observational evidence. If the ice sheet changes are, by definition, the central phenomenon of glacial-interglacial cycles, other components of the climate sys-tem (atmospheric CO2 concentration, Southern Ocean productivity, or global deep-ocean circulation) may play an even more fundamental role in these climatic cycles. 1