Chronostratigraphy of the 600,000 year old continental record of Lake Van (Turkey)

Stockhecke, Mona; Kwiecien, Ola; Vigliotti, L.; Anselmetti, Flavio S.; Beer, Jürg; Çağatay, M. Namık; Channell, James E T; Kipfer, Rolf; Lachner, Johannes; Litt, Thomas; Pickarski, Nadine; Sturm, Michael

doi:10.1016/j.quascirev.2014.04.008

Cited by 87 publications

(90 citation statements)

References 35 publications

(47 reference statements)

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“…This scenario includes the rising of the Northern Hemisphere summer insolation, leading to ice sheet melting and freshwater supply into the Atlantic Ocean (Denton et al, 2010). In this study, we follow the structure of TIII at 250 ka, TIIIA at 223 ka, and TII at 136 ka after Barker et al (2011) and Stockhecke et al (2014a;Figs. 3, 5).…”

Section: Boundary Definition and Biostratigraphymentioning

confidence: 97%

“…(f) Selected tree percentages (total arboreal pollen (AP), deciduous Quercus, and Pinus) including the pollen data from ; PAZ is pollen assemblage zone. Termination III at 250 ka, TIIIA at 223 ka, and TII at 136 ka are indicated after Barker et al (2011) and Stockhecke et al (2014a).…”

Section: The Oxygen Isotopic Composition Of Lake Van Sedimentsmentioning

confidence: 99%

“…The analytical approaches applied for the Lake Van chronology have previously been published in detail in Stockhecke et al (2014a) All ages are given in thousands of years before present (ka), where 0 before present is defined as 1950 AD. Marine isotope stage (MIS) boundaries follow Lisiecki and Raymo (2004).…”

Section: Chronologymentioning

confidence: 99%

“…Based on long continental records in southern Europe (compiled by Tzedakis et al, 1997Tzedakis et al, , 2001) and in the eastern Mediterranean area Stockhecke et al, 2014a), it was shown that there is a broad correspondence between warm climatic intervals, especially periods of low ice volume as defined by the marine isotope stage (MIS; Lisiecki and Raymo, 2004), and terrestrial temperate intervals (forested periods). In the continental semiarid Lake Van area, it is difficult to use only the expansion of trees as a criterion for the lower boundary of a warm stage.…”

Section: Boundary Definition and Biostratigraphymentioning

confidence: 99%

“…In the continental semiarid Lake Van area, it is difficult to use only the expansion of trees as a criterion for the lower boundary of a warm stage. Therefore, the climatic boundaries at Lake Van were mainly defined by abiotic proxies (i.e., TOC) caused by a higher time resolution (Stockhecke et al, 2014a). However, we are aware that using different proxies does not necessarily result in the same dates on the timescale (Sánchez Goñi et al, 1999;Shackleton et al, 2003).…”

Section: Boundary Definition and Biostratigraphymentioning

confidence: 99%

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A new high-resolution pollen sequence at Lake Van, Turkey: insights into penultimate interglacial–glacial climate change on vegetation history

Pickarski

Litt

2017

Clim. Past

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Abstract.A new detailed pollen and oxygen isotope record of the penultimate interglacial-glacial cycle, corresponding to the marine isotope stage (MIS) 7-6, has been generated from the Ahlat Ridge (AR) sediment core at Lake Van, Turkey. The presented Lake Van pollen record (ca. 250.2-128.8 ka) displays the highest temporal resolution in this region with a mean sampling interval of ∼ 540 years.The integration of all available proxies shows three temperate intervals of high effective soil moisture availability. This is evidenced by the predominance of steppe-forested landscapes (oak steppe-forest) similar to the present interglacial vegetation in this sensitive semiarid region between the Black Sea, the Caspian Sea, and the Mediterranean Sea.The wettest and warmest stage, as indicated by highest temperate tree percentages, can be broadly correlated with MIS 7c, while the amplitude of the tree population maximum during the oldest penultimate interglacial (MIS 7e) appears to be reduced due to warm but drier climatic conditions. The detailed comparison of the penultimate interglacial complex (MIS 7) to the last interglacial (Eemian, MIS 5e) and the current interglacial (Holocene, MIS 1) provides a vivid illustration of possible differences in the successive climatic cycles. Intervening periods of treeless vegetation can be correlated with MIS 7d and 7a, in which open landscapes favor local erosion and detrital sedimentation. The predominance of steppe elements (e.g., Artemisia, Chenopodiaceae) during MIS 7d indicates very dry and cold climatic conditions. In contrast, the occurrence of higher temperate tree percentages (mainly deciduous Quercus) throughout MIS 7b points to relatively humid and mild conditions, which is in agreement with other pollen sequences in southern Europe.Despite the general dominance of dry and cold desertsteppe vegetation during the penultimate glacial (broadly equivalent to MIS 6), this period can be divided into two parts: an early stage (ca. 193-157 ka) with higher oscillations in tree percentages and a later stage (ca. 157-131 ka) with lower tree percentages and subdued oscillations. This subdivision of the penultimate glacial is also seen in other pollen records from southern Europe (e.g., MD01-2444 and I-284;Margari et al., 2010;Roucoux et al., 2011). The occurring vegetation pattern is analogous to the division of MIS 3 and MIS 2 during the last glacial in the same sediment sequence. Furthermore, we are able to identify the MIS 6e event (ca. 179-159 ka) as described in marine pollen records, which reveals clear climate variability due to rapid alternation in the vegetation cover.In comparison with long European pollen archives, speleothem isotope records from the Near East, and global climate parameters (e.g., insolation, atmospheric CO 2 content), the new high-resolution Lake Van record presents an improved insight into regional vegetation dynamics and climate variability in the eastern Mediterranean region.

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Section: Boundary Definition and Biostratigraphymentioning

confidence: 97%

Section: The Oxygen Isotopic Composition Of Lake Van Sedimentsmentioning

confidence: 99%

Section: Chronologymentioning

confidence: 99%

Section: Boundary Definition and Biostratigraphymentioning

confidence: 99%

Section: Boundary Definition and Biostratigraphymentioning

confidence: 99%

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A new high-resolution pollen sequence at Lake Van, Turkey: insights into penultimate interglacial–glacial climate change on vegetation history

Pickarski

Litt

2017

Clim. Past

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Interglacials of the last 800,000 years

2016

Reviews of Geophysics

381

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Interglacials, including the present (Holocene) period, are warm, low land ice extent (high sea level), end-members of glacial cycles. Based on a sea level definition, we identify eleven interglacials in the last 800,000 years, a result that is robust to alternative definitions. Data compilations suggest that despite spatial heterogeneity, Marine Isotope Stages (MIS) 5e (last interglacial) and 11c (~400 ka ago) were globally strong (warm), while MIS 13a (~500 ka ago) was cool at many locations. A step change in strength of interglacials at 450 ka is apparent only in atmospheric CO 2 and in Antarctic and deep ocean temperature. The onset of an interglacial (glacial termination) seems to require a reducing precession parameter (increasing Northern Hemisphere summer insolation), but this condition alone is insufficient. Terminations involve rapid, nonlinear, reactions of ice volume, CO 2 , and temperature to external astronomical forcing. The precise timing of events may be modulated by millennial-scale climate change that can lead to a contrasting timing of maximum interglacial intensity in each hemisphere. A variety of temporal trends is observed, such that maxima in the main records are observed either early or late in different interglacials. The end of an interglacial (glacial inception) is a slower process involving a global sequence of changes. Interglacials have been typically 10-30 ka long. The combination of minimal reduction in northern summer insolation over the next few orbital cycles, owing to low eccentricity, and high atmospheric greenhouse gas concentrations implies that the next glacial inception is many tens of millennia in the future. Introduction-Interglacials of the Last 800 kaEarth's climate of the last 800 ka (1 ka = 1000 years) is the latest stage in a slow cooling that has been in progress for the last~50 Ma (1 Ma = 1 million years) [Zachos et al., 2008]. During this cooling, ice sheets formed on the Antarctic continent~40 Ma ago, while the first signs of Northern Hemisphere (NH) glaciation appeared much more recently. Only at the start of the Quaternary Period and the Pleistocene Epoch,~2.6 Ma ago, did alternations between cold glacial periods with ice on the NH continents, and warmer intervals with little or no NH continental ice, first appear, reflected in the appearance of ice-rafted debris Kleiven et al., 2002] and in enhanced amplitude of cyclicity in benthic oxygen isotopes in marine sediment records (Figure 1) [Lisiecki and Raymo, 2005].Somewhere between 1.2 and 0.6 Ma ago, weaker cycles with a period of~40 ka gave way to stronger (greater isotopic amplitude) cycles with a recurrence period closer to 100 ka. This change is known as the Mid-Pleistocene Transition or Revolution. Its exact date is debated, and it is likely that different aspects of climate shifted into their new mode of operation at different times [Mudelsee and Schulz, 1997;Rutherford and D'Hondt, 2000;Clark et al., 2006;Elderfield et al., 2012]. By 800 ka ago, the change in amplitude was complete in most re...

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Biomarkers in Lake Van sediments reveal dry conditions in eastern Anatolia during 110.000–10.000 years B.P.

Randlett

Bechtel

Meer

et al. 2017

Geochem Geophys Geosyst

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Lipid biomarkers were analyzed in Lake Van sediments covering the last 600 ka, with a focus on the period between 110 and 10 ka, when a broad maximum in pore water salinity as a relict from the past suggests dry conditions. The occurrence and distribution of biomarkers indicative for terrestrial plants (long‐chain n‐alkane C29), haptophyte algae (methyl alkenones C37) and halophilic archaea (archaeol) all point toward a dry climate in Lake Van region during this time interval. The hydrogen isotopic composition of C29 n‐alkanes (δDC29) and C37 alkenones (δDC37) is enriched between MIS 4 and MIS 2, which is interpreted as a decrease in the regional ratio of precipitation to evaporation. Similarly, the low abundance of the acyclic glycerol dialkyl glycerol tetraether GDGT‐0 relative to archaeol, quantified by the Archaeol and Caldarchaeol Ecometric (ACE) is assumed to reflect the presence of halophilic euryarchaeota adapted to high salinity water. The climate around Lake Van appears in phase with the Yammouneh basin 800 km southwest and Lake Urmia 250 km southeast of Lake Van over the last two glacial periods. The results highlight the potential of combining ACE, δDC29, and δDC37 for reconstructing salinity changes and regional precipitation to evaporation ratio from lake sediments.

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Chronostratigraphy of the 600,000 year old continental record of Lake Van (Turkey)

Cited by 87 publications

References 35 publications

A new high-resolution pollen sequence at Lake Van, Turkey: insights into penultimate interglacial–glacial climate change on vegetation history

A new high-resolution pollen sequence at Lake Van, Turkey: insights into penultimate interglacial–glacial climate change on vegetation history

Interglacials of the last 800,000 years

Biomarkers in Lake Van sediments reveal dry conditions in eastern Anatolia during 110.000–10.000 years B.P.

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