The two major warming phases of the last deglaciation at ∼14.7 and ∼11.5 ka cal BP in Europe: climate reconstructions and AGCM experiments

Renssen, H.; Isarin, R.F.B.

doi:10.1016/s0921-8181(01)00082-0

Cited by 164 publications

(172 citation statements)

References 74 publications

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“…During a warm episode around *14,700 cal year BP, air temperatures in ice-free regions of the Baltic Sea basin increased to values close to modern values. This can be inferred from data of changing vegetation (Hoek 2001) and is consistent with modelling results obtained by Renssen and Isarin (2001) with the general circulation model ECHAM4. In their study, ECHAM4 was driven by different reconstructions of sea surface temperature available at the time of publication, by changed orbital configuration and by reconstructions of vegetation cover.…”

Section: Climate At the Boundary Of The Younger Dryas/holocenesupporting

confidence: 89%

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: Climate At the Boundary Of The Younger Dryas/holocenesupporting

confidence: 89%

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

Борзенкова

Zorita

Borisova

et al. 2015

Regional Climate Studies

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“…This implies that the lake-level lowering is related to summer dryness, while river incision may be a result of increasing precipitation and higher discharge during the winter, or the snow melting season in addition to a possible impact of changes in vegetation cover (Vandenberghe, 2003). Conversely, the rise in lake level and the return of rivers to braided channels at the beginning of GS-1 suggest an opposite pattern of seasonality marked by wetter summers and drier winters as a result of a southward shift of (1) the sea ice during the winter and (2) the storm track in the summer in agreement with AGCM experiments (Renssen and Isarin, 2001;Renssen and Bogaart, 2003).…”

Section: Comparison Of the Quantitative Reconstructionssupporting

confidence: 78%

“…Regarding the quantitative reconstructions of climatic parameters, Table 4 presents a comparison of results obtained from the various methods used at Lautrey as well as (1) from pollen and cladocera-based transfer functions at Gerzensee in Switzerland (Lotter et al, 2000), (2) from coleopteran data in the Swiss Plateau (Gaillard and Lemdahl, 1994;Coope and Elias, 2000) and in the Paris Basin (Limondin-Lozouet et al, 2002), and (3) from geological-palaeoecological data and AGCM experiments in Europe (Isarin and Bohncke, 1999;Renssen and Isarin, 2001;Renssen and Bogaart, 2003). Additional data are provided by previous studies at Lake Le Locle in the Swiss Jura mountains ).…”

Section: Comparison Of the Quantitative Reconstructionsmentioning

confidence: 99%

“…This is paralleled by an abrupt increase in snow accumulation over the Greenland ice-sheet during the same period (Alley et al, 1993). Such a general reactivation of the hydrological cycle probably reflects the retreat of sea ice (Renssen and Isarin, 2001) and increased evaporation over the ocean due to higher temperatures. The phases of rapid warming at 14,700 and 11,500 cal yr BP were also characterised by a major lake-level lowering in the Jura mountains and on the Swiss Plateau and an important incision of valley floors in western Europe (Antoine, 1997;Vandenberghe, 2003).…”

Section: Comparison Of the Quantitative Reconstructionsmentioning

confidence: 99%

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Environmental and climatic changes in the Jura mountains (eastern France) during the Lateglacial–Holocene transition: a multi-proxy record from Lake Lautrey

Magny

Aalbersberg

Bégeot

et al. 2006

Quaternary Science Reviews

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This paper presents a multi-proxy reconstruction of the climatic and environmental changes during the Last Glacial-Interglacial transition as recorded by a sediment sequence from Lake Lautrey (Jura, eastern France). This reconstruction is based on analysis of pollen, chironomid, organic matter, oxygen-isotope, mineralogical, magnetic susceptibility and inferred lake-level data at a high temporal resolution. The chronology is derived using AMS radiocarbon dates, the position of the Laacher See Tephra (LST), and of correlation between the Lautrey and GRIP oxygen-isotope records. This data set reveals a detailed sequence of environmental changes in the Jura mountains from Greenland Stadial 2a to the early Holocene. Biotic and abiotic indicators allow the recognition of major abrupt changes associated with the GS2a/GI-1e, GI-1a/GS-1 and GS-1/Preboreal transitions, and other minor fluctuations related to the cold events GI-1d, GI-1b and the Preboreal oscillation (PBO). They also suggest additional cooling spells at ca 14,550 and 14,350 cal yr BP (Intra-Bølling Cold Periods), at ca 13,500 and ca 12,700 cal yr BP just before the GS-1 onset, and at ca 11,350 cal yr BP just before the PBO, as well as an intriguing brief warming episode within GS-1 at ca 12,080 cal yr BP. Summer temperature increased by ca 5 °C at the start of GI-1e, and by 1.5-3 °C at the Holocene onset, while it decreased by ca 3-4 °C at the beginning of GS-1. Major changes in local hydrology and in seasonality appear to be also associated with the GS-2a/GI1e, GI-1a/GS-1 and GS-1/Preboreal transitions. Pollen and abiotic indicators suggest a greater sensitivity of the vegetation cover to climatic oscillations during the first part of the Lateglacial Interstadial than during the second part (after ca 13,700 cal yr BP), when a closed forest had been restored in this area. By contrast, the restoration of forest cover took less than 300 yr after the end of GS-1. At the beginning of GI-1e and GS-1, no lag occurs (within the sampling resolution of 20-50 yr) in the responses of aquatic (chironomids) and terrestrial (pollen) ecosystems, while, at the onset of the Holocene, the response of the vegetation appears slightly delayed in comparison with that of the chironomid community. Finally, the recognition of two successive tephra layers, which were deposited just before the LST at ca 12,950 cal yr BP and which originated from Le Puy de la Nugère (Massif Central, France), provides an additional tephrochronological tool for correlation between Lateglacial European sequences.

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“…In our study area, changed partioning of Rhine discharge between the central course and the Oude IJssel valley may have further accentuated contraction and preservation of multiple Late Weichselian braidplain levels. The biostratigraphic results indicate that these braiding conditions continued over the Pleniglacial to Late Glacial transition (onset Bølling) despite the significant warming that occurred at this transition (Renssen & Isarin, 2001). It shows that contraction of flow into a narrower zone is a relative fast way of river response to a (hydrologically) changing climate.…”

Section: Late Pleniglacial Bølling and Older Dryasmentioning

confidence: 92%

Climate-driven fluvial development and valley abandonment at the last glacial-interglacial transition (Oude IJssel-Rhine, Germany)

Janssens

Kasse

Bohncke

et al. 2012

Netherlands Journal of Geosciences

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Although numerous studies have been performed on fluvial system change over the last glacial-interglacial transition, the response of river systems to allogenic (climate) and autogenic forcing mechanisms and timing of this response are still not completely understood (e.g. Starkel, 1983;Vandenberghe et al., 1995;Rose, 1995;Blum & Törnqvist, 2000;Gibbard & Lewin, 2002;Vandenberghe, 2008;Erkens, 2009). The valleys of the Rhine and the Maas in the Lower Rhine Embayment have a long research history on this topic (Pons,1957;Van de Meene, 1977;Verbraeck, 1984;Klostermann, 1992;Schirmer, 1995;Berendsen & Stouthamer, 2001;Cohen et al., 2002;Busschers et al., 2007;Erkens et al., 2011). In this area, a well-preserved terraced morphology exists, with OSL-datable fluvial sequences with aeolian cover and with palaeochannel fills that allow vegetation AbstractIn the Weichselian, the Lower Rhine in the Dutch-German border region has used three courses, dissecting ice-marginal topography inherited from the Saalian. In the Late Weichselian, the three courses functioned simultaneously, with the central one gaining importance and the outer ones abandoning. This study aims to reconstruct the fluvial development and forcings that culminated in abandonment of the northern branch 'Oude IJssel-Rhine', at the time of the Lateglacial to Holocene transition. The fluvial architecture is studied using a cored transect over the full width of the valley, detailed cross-sections over palaeochannels and geomorphological analysis using digital elevation and borehole data. Biostratigraphy, radiocarbon dating and OSL dating provide a timeframe to reconstruct the temporal fluvial development. In its phase of abandonment, the fluvial evolution of the Oude IJssel-Rhine course is controlled by the ameliorating climate and related vegetation and discharge changes, besides by intrinsic (autogenic) fluvial behaviour such as the competition for discharge with the winning central branch and the vicinity of the Lippe tributary confluence. The rapid climate warming at the start of the Late Glacial resulted in flow contraction as the initial response. Other fluvial geomorphic adjustments followed, with some delay. An aggrading braided or transitional system persisted until the start of the Allerød, when channel patterns finally changed to meandering. Floodplain incision occurred at the Allerød -Younger Dryas transition and a multi-channel system developed fed by Rhine discharge. At the start of the Holocene, this system transformed into a small-scale, local meandering system, which was abandoned shortly after the start of the Holocene.The final abandonment of the Oude IJssel-Rhine and Niers-Rhine courses can be attributed to deep incision of the Central Rhine course in the earliest Holocene and is considered to be controlled by flow contraction induced by climate and related vegetation and discharge changes.

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The two major warming phases of the last deglaciation at ∼14.7 and ∼11.5 ka cal BP in Europe: climate reconstructions and AGCM experiments

Cited by 164 publications

References 74 publications

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

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

Environmental and climatic changes in the Jura mountains (eastern France) during the Lateglacial–Holocene transition: a multi-proxy record from Lake Lautrey

Climate-driven fluvial development and valley abandonment at the last glacial-interglacial transition (Oude IJssel-Rhine, Germany)

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