Abstract
In this paper we propose a methodological sequence for the study of glaciers and climate change, and for the use of glaciers as indicators of climatic evolution. Our proposal includes different techniques focused on: mapping glacier extents at different dates, measuring front variations, calculating areas and volumes, analyzing glacier Equilibrium-Line Altitudes (ELA), statistical treatment of climate series, and the application of glacier-climate models that relate temperature and precipitation and enable paleoclimate reconstruction. This methodology was tested by remote monitoring of three highly sensitive debris-free glaciers in the Tröllaskagi peninsula (northern Iceland) since the end of the Little Ice Age (LIA), and the results show an average retreat of 1.3 km as well as a reduction in area and volume of 25% and 33% as a result of the warming that began at the end of the LIA. The application of the glacier-climate models suggests a climate that was up to 49% less humid at the LIA maximum. The bibliographic review of the methods utilized enables us to validate our methodological proposal and the results obtained, and ensures its application in different areas of study.
Highlights
Glaciers respond to climatic variability through changes in their length, area, volume, thickness and flow rate (Francou and Vincent, 2010; Gabbud et al, 2016)
The objective of this study is to propose and evaluate a methodological approach applied in a sensitive area where glaciers dynamically respond to the changes in the elements that make up the climate (Andrés et al, 2016), and applicable in any area of study
A good statistical correlation between retreat/advance ratios and summer temperature has been found in the literature (e.g. Kirkbride, 2002; Bradwell et al, 2004), it should be noted that variations of the front are not in themselves an indicator of climate change, since they depend on mass balance and on ice speed as it flows from the accumulation zone to the ablation zone (Gabbud et al, 2016)
Summary
Glaciers respond to climatic variability through changes in their length, area, volume, thickness and flow rate (Francou and Vincent, 2010; Gabbud et al, 2016) In this sense, they are highly sensitive to variations in summer temperature and winter precipitation, as these are the variables that to a greater extent control ablation and accumulation (see Ahlmann, 1924; Liestøl, 1967; Sutherland, 1984; Ohmura et al, 1992) respectively, and affect the sign of mass balance and largely –but not exclusively (Gabbud et al, 2016)– front dynamics. The records of glacier lengths, combined with climate sensitivity and response times, are valuable proxies for the reconstruction of temperature histories, as shown by Oerlemans (2005)
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