What happens in the atmosphere during stadial-interstadial transitions?

H. Renssen, P.W. Bogaart & R.F.B Isarin

Faculty of Earth and Life Sciences, Vrije Universiteit Amsterdam, The Netherlands

Introduction

In the North Atlantic region, the glacial climate was characterized by rapid and abrupt climate swings between cold stadial conditions and relatively warm interstadial conditions1-2 (often called Dansgaard-Oeschger cycles). During these climatic shifts, the temperature increased by 9°C within a few decades3-4. Stadial-interstadial transitions were most probably caused by changes in the strength of the thermohaline circulation in the North Atlantic Ocean5. Further study of these climatic shifts and their impact on the envrionment is important, as this provides information on the response of the geo-system during phases of rapid climate change. We have used an atmospheric general circulation model (AGCM) to study the change in atmospheric circulation during the last stadial-interstadial transition: the shift from the Late Pleniglacial to the Bølling at 14,700 yrs BP.

Model and experiments

The applied AGCM is the ECHAM4-T42 model6 of the Max Planck Institute for Meteorology in Hamburg, Germany. For this study, we conducted three experiments:
 

  1. CONTROL: a control simulation of the present-day climate
  2. BØLLING: a simulation with boundary conditions for the Bølling period
  3. LATE-PLENI: a simulation with boundary conditions for the Late Pleniglacial


The boundary conditions that were changed compared to CONTROL include surface ocean conditions (SSTs and sea ice), orbital parameters, atmospheric concentrations of trace gases, surface albedo, ice sheet extension and topography. In the figure below, the prescribed anomalies in boundary conditions for  LATE-PLENI and BØLLING are shown.


Boundary conditions in the North Atlantic region prescribed in experiments LATE-PLENI and BØLLING. Yellow denotes land-surfaces, blue land-ice and white ocean. The SSTs and ice-sheet elevations are plotted as anomalies compared to experiment CONTROL.
 

Surface temperature

The simulated surface air temperatures clearly reflect the influence of the prescribed changes in SSTs and sea ice cover. For instance, January temperatures increase by more than 40°C over the central North Atlantic, where a sea-ice cover is no longer present in the Bølling during winter. Over the adjacent continents, the warming is somewhat less, but still considerable.

Simulated increase in January surface air temperature (°C) over the 14,700 yr BP stadial-interstadial transition (BØLLING minus LATE PLENI)

The simulated temperature increase for NW Europe (15 to 25°C), is in agreement with reconstructions based on a variety of proxy data (see Renssen & Isarin, 2001), indicating that the set of boundary conditions prescribed in LATE-PLENI and BØLLING are based on reasonable assumptions. This suggests that we may use these experiments to study the changes in atmospheric circulation over a stadial-interstadial transition.

Sea level pressure

In experiment LATE-PLENI, the winter mean surface pressure over the ice-covered North Atlantic Ocean is relatively low due to the strong surface cooling and descending airflow. As a consequence, the Icelandic Low is not well developed. In BØLLING, on the other hand, the surface pressure distribution is similar to today with a strong Icelandic Low and a steep pressure gradient over the North Atlantic. Over NW Europe, however, the pressure gradient is steeper in LATE-PLENI than in BØLLING due to the more easterly position of the Icelandic Low under stadial conditions, producing stronger winds over the continent between 50 and 55°N in LATE-PLENI. Thus, over the ocean, the westerly winds become stronger during the stadial-interstadial transition, while over NW Europe the winds become weaker. The latter result is consistent with geological evidence7, showing a strong decrease in eolian deposition during last stadial-interstadial transitions.


These figures show the simulated winter sea level pressures (left panel) and wind speed (right panel, see scale bar in m/s). The surface pressures are shown as anomalies from the global mean to account for pressure differences related to the introduction of ice sheets.
 

Storm tracks

To analyze the changes in storm tracks, we high-pass filtered the standard deviations of the sea level pressure. In LATE-PLENI, the storm track was positioned along 55°N, following the main temperature gradient associated with the southern sea-ice margin. A clear west-east orientation is visible, indicating that depressions reached NW Europe very frequently. In contrast, the reduced sea-ice cover prescribed in BØLLING produced a main storm track with a southwest-northeast orientation, with depressions mainly travelling into the Nordic Seas area. Thus, our experiments suggest that NW Europe experienced a drastic decrease in storm activity during stadial-interstadial transitions.
 


Simulated storm tracks for experiments LATE-PLENI and BØLLING
Effect on temperature variability

The noted change in storm activity had a major influence on the temperature variability in NW Europe. In LATE-PLENI, the passage of a cyclone first brought relatively mild Atlantic air to the European continent with southwesterly winds, resulting in temperatures of 5°C. Subsequently, after the passage of the depression, northerly winds transported extremely cold air to NW Europe that originated from the sea-ice covered North Atlantic, producing temperatures around 40°C. Thus, within days, the temperature in NW Europe fluctuated between 40°C and 5°C. In BØLLING, the temperature fluctuations were much smaller, although during cold outbreaks the temperatures still reached 20°C and the mean winter value was around 7°C. A further important difference with LATE-PLENI is that during winter the temperatures regularly reached 3°C in BØLLING, thus causing frequent melting of the snow pack, whereas in LATE-PLENI the snow pack was able to build up throughout the winter.
 


Daily temperatures for one year, averaged over NW Europe. Note the strong variations in LATE-PLENI, which are associated with the passage of cyclones.
 

This difference caused substantial changes of the hydrology during stadial-interstadial transitions, as in LATE-PLENI the runoff peaked in spring during the melt of the thick snow pack, whereas in BØLLING the runoff was more evenly distributed over winter. This change in runoff is consistent with geological evidence suggesting that rivers in NW Europe changed from braided to meandering systems during stadial-interstadial transitions8. Consequently, our results suggest that the day-to-day temperature variability was strongly reduced in NW Europe during stadial-interstadial transitions, which had a strong impact on the surface hydrology here.

For further information, please consult the following papers

Renssen, H. & Isarin, R.F.B. (2001) The two major warming phases of the last deglaciation at ~14.7 and ~11.5 kyr cal BP in Europe: climate reconstructions and AGCM experiments. Global and Planetary Change30: 117-154.

Renssen, H. & Bogaart, P.W. (2003) Atmospheric variability over the ~14.7 kyr BP stadial-interstadial transition in the North Atlantic region as simulated by an AGCM. Climate Dynamics 20: 301-313.

References

  1. Johnsen, S. J., Clausen, H. B., Dansgaard, W., Fuhrer, K., Gundestrup, N., Hammer, C. U., Iversen, P., Jouzel, J., Stauffer, B., and Steffensen, J. P. (1992). Irregular glacial interstadials recorded in a new Greenland ice core. Nature 359, 311-313.
  2. Bond, G., Broecker, W., Johnsen, S., McManus, J., Labeyrie, L., Jouzel, J., and Bonani, G. (1993). Correlations between climate records from North Atlantic sediments and Greenland ice. Nature 365, 143-147.
  3. Koç, N., and Jansen, E. (1994). Response of the high-latitude Northern Hemisphere to orbital climate forcing: evidence from the Nordic Seas. Geology 22, 523-526.
  4. Severinghaus, J. P., and Brook, E. J. (1999). Abrupt climate change at the end of the last glacial period inferred from trapped air in polar ice. Science 286, 930-934.
  5. Ganopolski, A., and Rahmstorf, S. (2001). Rapid changes of glacial climate simulated in a coupled climate model. Nature 409, 153-158.
  6. Roeckner, E., Arpe, K., Bengtsson, L., Christoph, M., Claussen, M., Dümenil, L., Esch, M., Giorgetta, M., Schlese, U., and Schulzweida, U. (1996). The atmospheric general circulation model ECHAM-4: model description and simulation of present-day climate. Max-Planck-Institute für Meteorologie report no. 218, Hamburg, Germany, 90 pp..
  7. Kasse, C. (1997). Cold-climate aeolian sand-sheet formation in north-western Europe (c. 14-12.4 ka); a response to permafrost degradation and increased aridity. Permafrost and Periglacial Processes 8, 295-311.
  8. Huisink, M. (1997). Late-glacial sedimentological and morphological changes in a lowland river in response to climatic change: the Maas, southern Netherlands. Journal of Quaternary Science 12, 209-223.

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