Late-Quaternary summer temperature changes in the northern-European tree-line region

Seppä, Heikki; MacDonald, Glen M.; Birks, H. John B.; Gervais, Bruce R.; Snyder, Jeffrey A.

doi:10.1016/j.yqres.2008.02.002

Cited by 43 publications

(39 citation statements)

References 64 publications

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“…The calibration of a statistical transfer function for pollen data requires a collection of modern surface pollen samples that are mathematically correlated to modern climate parameters. Transfer functions have been developed for different parts of the Baltic Sea basin and can be applied to climate reconstructions in the Lateglacial-Holocene period (Seppä 1996;Seppä and Birks 2002;Seppä et al 2002aSeppä et al , b, 2004aSeppä et al , b, 2005Seppä et al , 2008Birks 2003;Seppä 2003, 2010;Antonsson 2006;Antonsson et al 2006Antonsson et al , 2008Antonsson and Seppä 2007;Birks and Seppä 2010). A calibrated pollen-climate model has been recently developed to quantitatively reconstruct the Holocene annual mean, summer and winter air temperatures in northern Europe and in the Baltic Sea region.…”

Section: Methodology For Palaeoclimatic Reconstructionsmentioning

confidence: 99%

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Climate Change During the Holocene (Past 12,000 Years)

Борзенкова

Zorita

Borisova

et al. 2015

Regional Climate Studies

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This chapter summarises the climatic and environmental information that can be inferred from proxy archives over the past 12,000 years. The proxy archives from continental and lake sediments include pollen, insect remnants and isotopic data. Over the Holocene, the Baltic Sea area underwent major changes due to two interrelated factors-melting of the Fennoscandian ice sheet (causing interplay between global sea-level rise due to the meltwater and regional isostatic rebound of the earth's crust causing a drop in relative sea level) and changes in the orbital configuration of the Earth (triggering the glacial to interglacial transition and affecting incoming solar radiation and so controlling the regional energy balance). The Holocene climate history showed three stages of natural climate oscillations in the Baltic Sea region: short-term cold episodes related to deglaciation during a stable positive temperature trend (11,000-8000 cal year BP); a warm and stable climate with air temperature 1.0-3.5°C above modern levels (8000-4500 cal year BP), a decreasing temperature trend; and increased climatic instability (last 5000-4500 years). The climatic variation during the Lateglacial and Holocene is reflected in the changing lake levels and vegetation, and in the formation of a complex hydrographical network that set the stage for the Medieval Warm Period and the Little Ice Age of the past millennium.

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Section: Methodology For Palaeoclimatic Reconstructionsmentioning

confidence: 99%

“…In central and southern Norway, the snow line (equilibrium line altitude) lowered by 200 m (Nesje and Dahl 2001;Nesje 2009). The altitude of the upper boundary of arboreal vegetation also lowered (Seppä and Birks 2001;Seppä et al 2007Seppä et al , 2008.…”

Section: The '82 Ka Cold Event'mentioning

confidence: 99%

Climate Change During the Holocene (Past 12,000 Years)

Борзенкова

Zorita

Borisova

et al. 2015

Regional Climate Studies

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“…Finally, the upper panel of Fig. 6 shows records indicating general climatic conditions in the Finnish Lapland as reflected by (1) (Seppä et al, 2008), (d) annual precipitation at Lake Svanåvatnet in northern Norway (Bjune and Birks, 2008), (e) winter precipitation at Jostedalsbreen in western Norway (Nesje et al, 2000), (f) lake-level records at Cerin in west-central Europe (Magny et al, 2011a), (g) at Lake Accesa in north-central Mediterranean (Magny et al, 2007), and (h) at Lake Preola in south-central Mediterranean (Magny et al, 2011b). Vertical grey bands indicate (i) the periods of disappearance of the Fennoscandian and Laurentide ice sheets (LIS) according to Renssen et al (2009), Jansson and Kleman (2004) and Törnqvist and Hijma (2012) with an episode of increasing sea-level rise around 7600 cal BP (Carlson et al, 2008), and (ii) a period of major climatic/palaeohydrological change around 4500-4000 cal BP.…”

Section: Millennial Trendsmentioning

confidence: 99%

“…pine megafossil in 200-yr intervals and (2) a chironomidinferred temperature record ( Seppä et al, 2008). In Fig.…”

Section: Climmentioning

confidence: 99%

North–south palaeohydrological contrasts in the central Mediterranean during the Holocene: tentative synthesis and working hypotheses

et al. 2013

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Abstract. On the basis of a multi-proxy approach and a strategy combining lacustrine and marine records along a north–south transect, data collected in the central Mediterranean within the framework of a collaborative project have led to reconstruction of high-resolution and well-dated palaeohydrological records and to assessment of their spatial and temporal coherency. Contrasting patterns of palaeohydrological changes have been evidenced in the central Mediterranean: south (north) of around 40° N of latitude, the middle part of the Holocene was characterised by lake-level maxima (minima), during an interval dated to ca. 10 300–4500 cal BP to the south and 9000–4500 cal BP to the north. Available data suggest that these contrasting palaeohydrological patterns operated throughout the Holocene, both on millennial and centennial scales. Regarding precipitation seasonality, maximum humidity in the central Mediterranean during the middle part of the Holocene was characterised by humid winters and dry summers north of ca. 40° N, and humid winters and summers south of ca. 40° N. This may explain an apparent conflict between palaeoclimatic records depending on the proxies used for reconstruction as well as the synchronous expansion of tree species taxa with contrasting climatic requirements. In addition, south of ca. 40° N, the first millennium of the Holocene was characterised by very dry climatic conditions not only in the eastern, but also in the central- and the western Mediterranean zones as reflected by low lake levels and delayed reforestation. These results suggest that, in addition to the influence of the Nile discharge reinforced by the African monsoon, the deposition of Sapropel 1 has been favoured (1) by an increase in winter precipitation in the northern Mediterranean borderlands, and (2) by an increase in winter and summer precipitation in the southern Mediterranean area. The climate reversal following the Holocene climate optimum appears to have been punctuated by two major climate changes around 7500 and 4500 cal BP. In the central Mediterranean, the Holocene palaeohydrological changes developed in response to a combination of orbital, ice-sheet and solar forcing factors. The maximum humidity interval in the south-central Mediterranean started ca. 10 300 cal BP, in correlation with the decline (1) of the possible blocking effects of the North Atlantic anticyclone linked to maximum insolation, and/or (2) of the influence of the remnant ice sheets and fresh water forcing in the North Atlantic Ocean. In the north-central Mediterranean, the lake-level minimum interval began only around 9000 cal BP when the Fennoscandian ice sheet disappeared and a prevailing positive NAO-(North Atlantic Oscillation) type circulation developed in the North Atlantic area. The major palaeohydrological oscillation around 4500–4000 cal BP may be a non-linear response to the gradual decrease in insolation, with additional key seasonal and interhemispheric changes. On a centennial scale, the successive climatic events which punctuated the entire Holocene in the central Mediterranean coincided with cooling events associated with deglacial outbursts in the North Atlantic area and decreases in solar activity during the interval 11 700–7000 cal BP, and to a possible combination of NAO-type circulation and solar forcing since ca. 7000 cal BP onwards. Thus, regarding the centennial-scale climatic oscillations, the Mediterranean Basin appears to have been strongly linked to the North Atlantic area and affected by solar activity over the entire Holocene. In addition to model experiments, a better understanding of forcing factors and past atmospheric circulation patterns behind the Holocene palaeohydrological changes in the Mediterranean area will require further investigation to establish additional high-resolution and well-dated records in selected locations around the Mediterranean Basin and in adjacent regions. Special attention should be paid to greater precision in the reconstruction, on millennial and centennial timescales, of changes in the latitudinal location of the limit between the northern and southern palaeohydrological Mediterranean sectors, depending on (1) the intensity and/or characteristics of climatic periods/oscillations (e.g. Holocene thermal maximum versus Neoglacial, as well as, for instance, the 8.2 ka event versus the 4 ka event or the Little Ice Age); and (2) on varying geographical conditions from the western to the eastern Mediterranean areas (longitudinal gradients). Finally, on the basis of projects using strategically located study sites, there is a need to explore possible influences of other general atmospheric circulation patterns than NAO, such as the East Atlantic–West Russian or North Sea–Caspian patterns, in explaining the apparent complexity of palaeoclimatic (palaeohydrological) Holocene records from the Mediterranean area.

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“…The ques tion of en vi ron men tal sta bil ity dur ing the Eemian Inter gla cial has long been dis cussed (Velichko et al, 1982(Velichko et al, , 2005Fronval and Jansen, 1996;Litt et al, 1996;Kukla et al, 1997Kukla et al, , 2002Seidenkrantz and Knudsen, 1997;Saarnisto et al, 1999;Guiter et al, 2003;Klotz et al, 2003Klotz et al, , 2004Kühl and Litt, 2003;Seppä et al, 2008, and oth ers). The dis cus sions widened when a re cord of strong tem per a ture fluc tu a tions dur ing the Eemian Inter gla cial was dis cov ered in ice cores in Greenland (Anklin et al, 1993;Dansgaard et al, 1993;Grootes et al, 1993;GRIP, 1993).…”

Section: Introductionmentioning

confidence: 99%