Younger Dryas deglaciation at Mt. Billingen, and clay varve dating of the Younger Dryas/Preboreal transition

• Published in: Boreas
• Main Author: STRÖMBERG, BO
• Format: Article in Journal/Newspaper
• Language: English
• Published: Wiley 1994
• Subjects: GISP; Greenland; Greenland ice cores; GRIP
• Online Access: http://dx.doi.org/10.1111/j.1502-3885.1994.tb00598.x; https://api.wiley.com/onlinelibrary/tdm/v1/articles/10.1111%2Fj.1502-3885.1994.tb00598.x; https://onlinelibrary.wiley.com/doi/pdf/10.1111/j.1502-3885.1994.tb00598.x

A clay varve chronology has been established for the Late Weichselian ice recession east of Mt. Billingen in Västergötland, Sweden. In this area the Middle‐Swedish end moraine zone was built up as a consequence of cold climate during the Younger Dryas stadial. A change‐over from rapid to slow retreat as a result of climatic deterioration at the Alleröd/Younger Dryas transition cannot be traced with certainty in the varve sequences, but it seems to have taken place just before 11,600 varve years BP. The following deglaciation was very slow for about 700 years — within the Middle‐Swedish end moraine zone the annual ice‐front retreat was only c . 10 m on average. A considerable time‐lag is to be expected between the Younger Dryas climatic event and this period of slow retreat. The 700 years of slow retreat were succeeded by 200 years of more rapid recession, about 50–75 m annually, and then by a mainly rapid and uncomplicated retreat of the ice‐front by 100–200 m/year or more, characterizing the next 1500 years of deglaciation in south and central Sweden. The change from about 50–75 m to 100–200 m of annual ice‐front retreat may reflect the Younger Dryas/Preboreal transition. Clay‐stratigraph‐ically defined, the transition is dated at c . 10,740 varve years BP, with an error of +100 to ‐250 years. In the countings of ice layers in Greenland ice cores (GRIP and GISP‐2) the end of the Younger Dryas climatic event is 800–900 years older. However, a climatic amelioration after the cold part of the Younger Dryas and in early Preboreal should rapidly be reflected by for example chemical components and dust in Greenland ice cores, and by increasing δ 13 C content in tree rings. On the other hand, the start of a rapid retreat of the inland ice margin can be delayed by several centuries. This can explain at least a part of the discrepancy between the time‐scales.