Oxygen isotopes of lake marl at Gerzensee and Leysin (Switzerland), covering the Younger Dryas and two minor oscillations, and their correlation to the GRIP ice core

Schwander, Jakob; Eicher, Ueli; Ammann, Brigitta

doi:10.1016/s0031-0182(00)00085-7

Cited by 177 publications

(134 citation statements)

References 41 publications

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“…The record indicates a climatic warming at around 17,500 cal yr BP connected to the expansion of Larix and Pinus cembra trees (Wick, 2004). Given the close connection between the Alpine-Central European and Greenland climatic histories (von Grafenstein et al, 1999Grafenstein et al, , 2000Schwander et al, 2000;Heiri and Millet, 2005) during the Lateglacial, the climatic warming at 17,500 cal yr BP may correspond to the positive excursion in the oxygen isotopes of the GRIP ice-core at ca 17,500-17,000 cal yr BP (maximum values in the younger half of GS-2b, Bjo¨rck et al, 1998). Despite the fact that Alpine glaciers reached the lowland edges of the Po-Plain during the LGM at ca 22,000 cal BP, the presence of woody taxa seems most likely for sheltered sites in the Po-Plain (e.g.…”

Section: Alpine Deglaciation and Vegetational And Climatic Processes mentioning

confidence: 99%

“…For this period non-pollen evidence of climatic change is still very rare south of the Alps, but several paleoclimatic records from the Northern Alpine forelands point to strong climatic oscillations during this period, which are also recorded in the Greenland ice cores Ammann et al, 2000;Brooks, 2000;Schwander et al, 2000;Heiri and Millet, 2005). For this period the paleoclimatic series from the Alps and Greenland document a pronounced general climatic cooling event reaching about À1.5 to À2 1C in and around the Alps at ca 13,100-12,900 cal yr BP.…”

Section: Climatic and Vegetational Changes At Ca 14500 Cal Yr Bpmentioning

confidence: 99%

“…the interval between the end of the Last Glacial Maximum (LGM) at 18,000 cal yr BP (Lambeck et al, 2002;Sarnthein et al, 2003;Kucera et al, 2005) and the beginning of the Holocene (i.e. 11,550 cal yr BP, Schwander et al, 2000). Although the southern slope of the Alps was extensively glaciated during the LGM (Ehlers and Gibbard, 2004), conifer and several broad-leaved tree species survived in the Po Plain and along the southeastern Alpine border .…”

Section: Introductionmentioning

confidence: 99%

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Interactions between climate and vegetation during the Lateglacial period as recorded by lake and mire sediment archives in Northern Italy and Southern Switzerland

Vescovi

Ravazzi

Arpenti

et al. 2007

Quaternary Science Reviews

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153

139

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We reconstruct the vegetational history of the southern side of the Alps at 18,000-10,000 cal yr BP using previous and new AMS-dated stratigraphic records of pollen, stomata, and macrofossils. To address potential effects of climatic change on vegetation, we compare our results with independent paleoclimatic series (e.g. isotope and chironomid records from the Alps and the Alpine forelands). The period before 16,000 cal yr BP is documented only at the lowland sites. The previous studies used for comparison with our new Palughetto record, however, shows that Alpine deglaciation must have started before 18,000-17,500 cal yr BP south of the Alps and that deglaciated sites were colonized by open woods and shrublands (Juniperus, tree Betula, Larix, Pinus cembra) at ca 17,500 cal yr BP. The vegetational history of a new site (Palughetto, 1040 m a.s.l.) is consistent with that of previous investigations in the study region. Our results show three conspicuous vegetational shifts delimited by statistically significant pollen zones, at ca 14,800-14,400, 13,300-12,800 and 11,600-11,200 cal yr BP. At sites situated above 1000 m a.s.l. (e.g. Palughetto, Pian di Gembro) forests expanded in alpine environments at ca 14,500 cal yr BP (onset of Bølling period, GI-1 in the Greenland ice record). At the same time, rather closed treeline communities of the lowlands were replaced by dense stands of Pinus sylvestris and Betula. These early forests and shrublands consisted of Larix, P. cembra, Juniperus, P. sylvestris, Pinus mugo, and Betula, and had become established at ca 16,000 cal yr BP, probably in response to a temperature increase. If combined with other records from the Southern Alps, our data suggest that treeline ascended by ca 800-1000 m in a few centuries at most, probably as a consequence of climatic warming at the beginning of the Bølling period. At 13,100-12,800 cal yr BP the onset of a long-lasting decline of P. sylvestris was accompanied by the expansion of Quercus and other thermophilous tree taxa below ca 600 m a.s.l. This vegetational change was probably induced by a shift to warmer climatic conditions before the onset of the Younger Dryas, as indicated by independent paleoclimatic records. Only a few centuries later, at ca 12,700-12,500 cal yr BP, an expansion of herbaceous taxa occurred in the lowlands as well as at higher altitudes, documenting an opening of forested habitats. This change coincided with the beginning of the Younger Dryas cooling (GS-1), which according to the paleoclimatic series (e.g. oxygen isotope series), started at 12,700-12,600 cal yr BP and lasted for about 1000 years. Environments south of the Alps responded markedly to climatic warming at the onset of the Holocene (11,600-11,500 cal yr BP). Thermophilous trees that had declined during the Younger Dryas re-expanded very rapidly in the lowlands and reached the high altitude sites below ca 1500 m a.s.l. within a few centuries at most. Our study implies that the synchronous vegetational changes observed over wide areas were probabl...

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Section: Alpine Deglaciation and Vegetational And Climatic Processes mentioning

confidence: 99%

Section: Climatic and Vegetational Changes At Ca 14500 Cal Yr Bpmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Interactions between climate and vegetation during the Lateglacial period as recorded by lake and mire sediment archives in Northern Italy and Southern Switzerland

Vescovi

Ravazzi

Arpenti

et al. 2007

Quaternary Science Reviews

Self Cite

153

139

View full text Add to dashboard Cite

show abstract

“…Early-Holocene temperatures were generally high at the beginning of the Holocene in the northern Alps and northern Europe (Porinchu and Cwynar, 2000;Stefanova et al, 2003;Caseldine et al, 2003;Heiri et al, 2004Heiri et al, , 2003Larocque and Hall, 2004). Mean annual temperature in and around the Alps increased by ca 3-6°C in the early Holocene (Eicher, 1994;Schwander et al, 2000). Instead, the amplitude of temperature increase at LPA was about 2.5°C, which is slightly smaller than at higher latitudes but similar to the amplitude recorded at Lago di Lavarone (Heiri et al, in press).…”

Section: Patterns Of Climatic Change As Inferred From Chironomid Recomentioning

confidence: 99%

Late-glacial chironomid-based temperature reconstructions for Lago Piccolo di Avigliana in the southwestern Alps (Italy)

Larocque

Finsinger

2008

Palaeogeography, Palaeoclimatology, Palaeoecology

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Chironomid headcapsules were used to reconstruct late glacial and early-Holocene summer temperatures at Lago Piccolo di Avigliana (LPA). Two training sets (northern Sweden, North America) were used to infer temperatures. The reconstructed patterns of temperature change agreed well with the GRIP and NGRIP δ 18 O records. Inferred temperatures were high during the Bølling (ca 19°C), slowly decreased to ca 17.5°C during the Allerød, reached lowest temperatures (ca 16°C) during the Younger Dryas, and increased to ca. 18.5°C during the Preboreal. The amplitudes of change at climate transitions (i.e. Oldest Dryas/Bølling: 3°C, Allerød/Younger Dryas: 1.5°C, and Younger Dryas/Preboreal: 2.5°C) were smaller than in the northern Alps but similar to those recorded at another site in northeastern Italy. Our results suggest that (1) Allerød temperatures were higher in the southern Alps and (2) higher during the Preboreal (1°C) than during the Allerød. These differences might provide an explanation for the different responses of terrestrial-vegetation to late glacial and early-Holocene climatic changes in the two regions. Other sites on both sides of the Alps should be studied to confirm these two hypotheses.

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“…For the LST an age of 12,900 cal yrs BP was adopted, following Baales et al (2002). This age scarcely differs from the 12,836 GRIP years age obtained by Schwander et al (2000) for the Gerzensee and Leysin records. Sediment changes in the analysed core are described in Finsinger (2004).…”

Section: Methodsmentioning

confidence: 99%

The late glacial–Holocene transition as inferred from ostracod and pollen records in the Lago Piccolo di Avigliana (Northern Italy)

Belis¹,

Finsinger

Ammann

2008

Palaeogeography, Palaeoclimatology, Palaeoecology

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Ostracod and pollen records of Lago Piccolo di Avigliana were used for the reconstruction of aquatic and terrestrial palaeoenvironments between 17 and 10 kyr cal BP. A combination of multivariate ordination techniques (PCA and RDA) made it possible to describe ostracod and pollen biostratigraphies and to evaluate whether changes in the aquatic ecosystem were associated with those in the terrestrial environments. Samples and taxa in the ordination plots were grouped into three clusters: a first cluster representing herbaceous and shrub pollen taxa (Juniperus, Chenopodiaceae, Gramineae, Artemisia, and Rubiaceae) associated with ostracods typical of oligotrophic and well oxygenated aquatic environments (Cytherissa lacustris), a second cluster containing pollen taxa representing boreal forests (Betula, Pinus sylvestris, and Pinus cembra) associated with ostracod taxa from shallow oligomesotrophic aquatic environments (Candona candida, Darwinula stevensoni), and a third cluster including pollen of thermophilous trees and shrubs (Corylus, Quercus ilex, Fraxinus, Quercus robur-type, and Ulmus) connected to ostracods representing warm mesotrophic aquatic conditions with aquatic vegetation (Cypria ophtalmica, Metacypris cordata). Hypothesis testing with constrained Monte Carlo permutations rejected the null hypothesis that no relationship exists between ostracod and pollen datasets at 2% level of significance. As a whole, changes in temperature and precipitation-evaporation balance that influenced terrestrial vegetation were represented by changes in trophic level and water level in the aquatic environment.

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Oxygen isotopes of lake marl at Gerzensee and Leysin (Switzerland), covering the Younger Dryas and two minor oscillations, and their correlation to the GRIP ice core

Cited by 177 publications

References 41 publications

Interactions between climate and vegetation during the Lateglacial period as recorded by lake and mire sediment archives in Northern Italy and Southern Switzerland

Interactions between climate and vegetation during the Lateglacial period as recorded by lake and mire sediment archives in Northern Italy and Southern Switzerland

Late-glacial chironomid-based temperature reconstructions for Lago Piccolo di Avigliana in the southwestern Alps (Italy)

The late glacial–Holocene transition as inferred from ostracod and pollen records in the Lago Piccolo di Avigliana (Northern Italy)

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