Across scale temperature modelling using a simple approach for the characterization of high mountain ecosystem complexity

Loeffler, Joerg

doi:10.3112/erdkunde.2004.04.04

Cited by 9 publications

(5 citation statements)

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“…Fjeldskaar, 1994;Helle et al, 2007). An initial strong uplift during Allerød halted during the Younger Dryas and resumed after its termination with high uplift rates in the Early Holocene that subsequently significantly decreased (Lohne et al, 2007). According to newest modelling by Fjeldskaar and Amatonov (2018) the calculated uplift between Allerød and Younger Dryas at around Dalsnibba would summarize to around 50 m, i.e.…”

Section: Exposure Age Calculationsmentioning

confidence: 99%

“…It has been debated whether the summit was covered by cold-based ice 168 P. Marr et al: 10 Be-based exploration of the timing of deglaciation Figure 1. Study areas in southern Norway and the location of Dalsnibba in the west and Blåhø in the east (modified after Löffler and Pape, 2004). (Goehring et al, 2008) or remained ice-free during the LGM (Nesje et al, 1994).…”

Section: Introductionmentioning

confidence: 99%

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<sup>10</sup>Be-based exploration of the timing of deglaciation in two selected areas of southern Norway

Marr

Winkler

Binnie

et al. 2019

E&G Quaternary Sci. J.

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Abstract. We present new 10Be surface exposure ages from two selected locations in southern Norway. A total of five 10Be samples allow a first assessment of local deglaciation dynamics of the Scandinavian Ice Sheet at Dalsnibba (1476 m a.s.l.) in southwestern Norway. The bedrock ages from the summit of Dalsnibba range from 13.3±0.6 to 12.7±0.5 ka and probably indicate the onset of deglaciation as a glacially transported boulder age (16.5±0.6 ka) from the same elevation likely shows inheritance. These ages indicate initial deglaciation commencing at the end of the Bølling–Allerød interstadial (∼ 14.7–12.9 kyr BP) and ice-free conditions at Dalsnibba's summit during the Younger Dryas. Bedrock samples at lower elevations imply vertical ice surface lowering down to 1334 m a.s.l. at 10.3±0.5 ka and a longer overall period of downwasting than previously assumed. Two further 10Be samples add to the existing chronology at Blåhø (1617 m a.s.l.) in south-central Norway. The 10Be erratic boulder sample on the summit of Blåhø sample yields 20.9±0.8 ka, whereas a 10Be age of 46.4±1.7 ka for exposed summit bedrock predates the Late Weichselian Maximum. This anomalously old bedrock age infers inherited cosmogenic nuclide concentrations and suggests low erosive cold-based ice cover during the Last Glacial Maximum. However, due to possible effects of cryoturbation and frost heave processes affecting the erratic boulder age and insufficient numbers of 10Be samples, the glaciation history on Blåhø cannot conclusively be resolved. Comparing the different timing of deglaciation at both locations in a rather short west–east distance demonstrates the complex dynamics of deglaciation in relation to other areas in southern Norway.

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Section: Exposure Age Calculationsmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

<sup>10</sup>Be-based exploration of the timing of deglaciation in two selected areas of southern Norway

Marr

Winkler

Binnie

et al. 2019

E&G Quaternary Sci. J.

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“…117-128 E 2010 Regents of the University of Colorado D. WUNDRAM ET AL. / 117 1523-0430/10 $7.00 and Pape, 2004;Lö ffler and Finch, 2005;Pape et al, 2009). That being so, taking nonlinearities of climate systems into consideration was found to be of greater importance when assessing the impact of global climatic change on mountain ecosystems (Peterson, 2000;Diaz et al, 2003;Rial et al, 2004).…”

Section: Introductionmentioning

confidence: 99%

Alpine Soil Temperature Variability at Multiple Scales

Wundram

Pape

Löffler

2010

Arctic, Antarctic, and Alpine Research

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“…However, regional climate reconstructions might be affected by local site‐specific topographic factors that are characteristic of alpine environments. In alpine regions, topography strongly controls microclimate (Barry, 1992; Löffler & Pape, 2004; Löffler et al. , 2006).…”

Section: Introductionmentioning

confidence: 99%

Growth‐ring variations of dwarf shrubs reflect regional climate signals in alpine environments rather than topoclimatic differences

Bär

Pape

Bräuning

et al. 2007

Journal of Biogeography

104

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Aim Our main aim is to determine if ring-width variations in Empetrum hermaphroditum reflect regional or local topoclimate signals in an alpine environment. In the case that topoclimate provides the dominant signal, a secondary aim is to link these to spatial distribution patterns of different vegetation types.Location The study area is situated in the middle alpine belt in the Vågåmo region, Central Norwegian Scandes. Sampling sites cover different topoclimates: ridges, north-facing slopes and south-facing slopes.Methods We constructed ring-width chronologies of E. hermaphroditum for each type of microsite for the common period 1951-2004. Climate data were prepared on an hourly, daily and growing-season time scale. Climate-growth relationships were evaluated using bivariate correlations and regression tree methods for continuous time-series analyses. In addition, extreme growth anomalies (pointer years) were compared with the climate conditions in those years. The impact of water supply on wood anatomy was determined by correlating the conductive area (percentage of vessel per growth ring) with a running mean (sum) of 10-day intervals for temperature and precipitation.Results This study indicates that mean summer (June-August) temperatures determine the width of the growth rings of E. hermaphroditum irrespective of topoclimate. The length of the growing season, which is the most differentiating climatic factor between microsites, does not substantially alter the anatomical ring structure. Microsite differences in mean growth rates are attributed to the higher frequency of warm days. Extremely warm days limit ring-width development at south-facing slopes, while plants at ridges and north-facing slopes still benefit from higher temperatures. As a consequence, pointer years are not developed synchronously at all microsites. Vessel formation is affected by available moisture, especially in the later part of the growing season.Main conclusions Topoclimate induces slight modifications of annual growthring increments of E. hermaphroditum at different microsites. In contrast to the distribution patterns of vegetation types that are determined by snow cover, growth-ring variations are related to summer temperature conditions, and the prominent regional climate signal is still reflected at all microsites. This offers the opportunity to reconstruct climatic change in alpine regions from dwarf shrub ring-width chronologies.

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Across scale temperature modelling using a simple approach for the characterization of high mountain ecosystem complexity

Cited by 9 publications

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<sup>10</sup>Be-based exploration of the timing of deglaciation in two selected areas of southern Norway

<sup>10</sup>Be-based exploration of the timing of deglaciation in two selected areas of southern Norway

Alpine Soil Temperature Variability at Multiple Scales

Growth‐ring variations of dwarf shrubs reflect regional climate signals in alpine environments rather than topoclimatic differences

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Across scale temperature modelling using a simple approach for the characterization of high mountain ecosystem complexity

Cited by 9 publications

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&lt;sup&gt;10&lt;/sup&gt;Be-based exploration of the timing of deglaciation in two selected areas of southern Norway

&lt;sup&gt;10&lt;/sup&gt;Be-based exploration of the timing of deglaciation in two selected areas of southern Norway

Alpine Soil Temperature Variability at Multiple Scales

Growth‐ring variations of dwarf shrubs reflect regional climate signals in alpine environments rather than topoclimatic differences

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<sup>10</sup>Be-based exploration of the timing of deglaciation in two selected areas of southern Norway

<sup>10</sup>Be-based exploration of the timing of deglaciation in two selected areas of southern Norway