Late Holocene diatom assemblages in a lake-sediment core from Central Kamchatka, Russia

Hoff, Ulrike; Dirksen, Oleg; Dirksen, V.; Herzschuh, Ulrike; Hubberten, Hans‐Wolfgang; Meyer, Hanno; Bogaard, Christel van den; Diekmann, Bernhard

doi:10.1007/s10933-012-9580-y

Cited by 14 publications

(22 citation statements)

References 39 publications

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“…Thereby, termination of cooling at the beginning of late Holocene is relatively synchronous in central Kamchatka, South Kurile, Bering and Japanese Islands (this study; Savoskul and Zech, 1997;Savoskul, 1999;Razjigaeva et al, 2004;Dirksen and Dirksen, 2008;Hoff et al, 2012) and take place around 3700 cal years BP. From ca 3700 cal years BP to the last millennium, a newly strengthened climate continentality accompanied by general warming trend with minor cool excursions led to apparent spatial heterogeneity of climatic patterns.…”

Section: To 160 Cal Years Bpmentioning

confidence: 59%

“…Diatom record of the upper part of the sediment record of the lake Sigrid, located near the TYL, showed that the last 500 years were likely characterized by summer cooling and may represent the Little Ice Age (Hoff et al, 2012). Pollen spectra in peat sections along the Pacific coast of Kamchatka also indicate climate deterioration after 1550 BC (Dirksen and Uspenskaya, 2005).…”

Section: To 160 Cal Years Bpmentioning

confidence: 99%

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Late Holocene climate and environmental changes in Kamchatka inferred from the subfossil chironomid record

Nazarova

Hoog

Hoff

et al. 2013

Quaternary Science Reviews

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Section: To 160 Cal Years Bpmentioning

confidence: 59%

Section: To 160 Cal Years Bpmentioning

confidence: 99%

Late Holocene climate and environmental changes in Kamchatka inferred from the subfossil chironomid record

Nazarova

Hoog

Hoff

et al. 2013

Quaternary Science Reviews

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“…Diatom taxonomy and purification for stable isotope analysis TYL sediment samples were freeze-dried and split into subsamples for micropalaeontological, sedimentological, and stable isotope studies. The sample preparation for quantitative diatom analyses (using light microscopy at 1000× magnification with a Zeiss AXIO A1 with an Achroplan 100× 1.4 Oil Ph3-objective and scanning electron microscopy) as well as diatom counting are described in detail in Hoff et al (2012;this issue). Due to the predominance of two diatom species (Aulacoseira subarctica (O. Müller) Haworth and Stephanodiscus minutulus (Kützing) Cleve & Möller) in the samples of TYL we needed to count up to a number of 300 frustules including every diatom species except the dominant two species (which have been counted along).…”

Section: Water Analysismentioning

confidence: 99%

Oxygen isotope composition of diatoms as Late Holocene climate proxy at Two-Yurts Lake, Central Kamchatka, Russia

Meyer

Chapligin

Hoff

et al. 2015

Global and Planetary Change

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Especially in combination with other proxies, the oxygen isotope composition of diatom silica (δ 18 O diatom ) from lake sediments is useful for interpreting past climate conditions. This paper presents the first oxygen isotope data of fossil diatoms from Kamchatka, Russia, derived from sediment cores from Two-Yurts Lake (TYL). For reconstructing Late Holocene climate change, palaeolimnological investigations also included diatom, pollen and chironomid analysis. The most recent diatom sample (δ 18 O diatom = +23.3‰) corresponds well with the present day isotopic composition of the TYL water (mean δ 18 O = −14.8‰) displaying a reasonable isotope fractionation in the system silicawater. Nonetheless, the TYL δ 18 O diatom record is mainly controlled by changes in the isotopic composition of the lake water. TYL is considered as a dynamic system triggered by differential environmental changes closely linked with lake-internal hydrological factors. The diatom silica isotope record displays large variations in δ 18O diatom from +27.3‰ to +23.3‰ from about 4.5 kyr BP until today. A continuous depletion in δ 18O diatom of 4.0‰ is observed in the past 4.5 kyr, which is in good accordance with other hemispheric environmental changes (i.e. a summer insolation-driven Mid-to Late Holocene cooling). The overall cooling trend is superimposed by regional hydrological and atmospheric-oceanic changes. These are related to the interplay between Siberian High and Aleutian Low as well as to the ice dynamics in the Sea of Okhotsk. Additionally, combined δ 18O diatom and chironomid interpretations provide new information on changes related to meltwater input to lakes. Hence, this diatom isotope study provides further insight into hydrology and climate dynamics of this remote, rarely investigated area.

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“…There has been recent interest in the Holocene palaeoenvironmental history of the Kamchatka Peninsula with most studies largely focusing on lakes and peat deposits in the southern and central parts of the Global and Planetary Change xxx (2015) xxx-xxx peninsula (e.g., Dirksen et al, 2011Dirksen et al, , 2013Hoff et al, 2012Hoff et al, , 2014). The climate model experiments suggest that mid-Holocene climatic changes were time-transgressive in the Kamchatka Peninsula with the Holocene thermal maximum (HTM) being delayed in southern and central Kamchatka by about 2000 years in comparison with northern Kamchatka, Alaska and NE Siberia (e.g., see Fig.…”

Section: Introductionmentioning

confidence: 99%

The Holocene environmental history of a small coastal lake on the north-eastern Kamchatka Peninsula

Solovieva

Klimaschewski

Self

et al. 2015

Global and Planetary Change

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a b s t r a c t a r t i c l e i n f oAvailable online xxxx A radiocarbon and tephra-dated sediment core from Lifebuoy Lake, located on the north-east coast of Kamchatka Peninsula, was analysed for pollen, spores, diatoms, chironomids and tephra in order to uncover regional environmental history. The 6500-year environmental history of Lifebuoy Lake correlates with the broad regional patterns of vegetation development and climate dynamics with both diatoms and chironomids showing near-synchronous changes. Between ca. 6300 and 3900 cal yr BP, the lake ecosystem was naturally enriched, with several Stephanodiscus species dominating the diatom plankton. This natural eutrophication state is likely to be due to a combination of the base-rich catchment geology, the fertilisation effect of several fires in the catchment, silica input from tephra layers and, possibly, nitrogen input from seabirds. The substantial tephra deposit at about 3850 cal yr BP might have stopped sedimentary phosphorus from entering the lake water thus decreasing the trophic state of the lake and facilitating the shift in diatom composition to a benthic Fragiliariaceae complex. Both diatoms and chironomids showed simultaneous compositional changes, which are also reflected by statistically significant changes in their rates of change 300-400 years after the arrival of Pinus pumila in the lake catchment. The rapid increase in both total diatom concentration and the percentage abundance of the large heavy species, Aulacoseira subarctica might be a response to the change in timing and intensity of lake spring turnover due to the changes in the patterns of North Pacific atmospheric circulation, most notably westward shift of the Aleutian Low. The two highest peaks in A. subarctica abundance at Lifebouy Lake occurred during opposite summer temperature inferences: the earlier peak (3500-2900 cal yr BP) coincided with warm summers and the latter peak (300 cal yr BP-present) occurred during the cold summer period. These imply that A. subarctica shows no direct response to the changes of summer air temperature. Instead, it appears to thrive during the periods of increased winter precipitation, thicker ice and late spring turn-over periods, i.e., shows indirect response to climate. The clearest effect of tephra deposition on the lake ecosystem is above 908 cm (ca. 3800 cal yr BP) where the tephra deposit might have caused the shift from Stephanodiscus-dominated planktonic assemblages to the Fragilariaceae complex of benthic species. Tephra deposits might have also contributed towards the development of eutrophic plankton from about 6300 cal yr BP. It is not certain if several tephra deposits influenced diatom and chironomid changes during the last 300 years.

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Late Holocene diatom assemblages in a lake-sediment core from Central Kamchatka, Russia

Cited by 14 publications

References 39 publications

Late Holocene climate and environmental changes in Kamchatka inferred from the subfossil chironomid record

Late Holocene climate and environmental changes in Kamchatka inferred from the subfossil chironomid record

Oxygen isotope composition of diatoms as Late Holocene climate proxy at Two-Yurts Lake, Central Kamchatka, Russia

The Holocene environmental history of a small coastal lake on the north-eastern Kamchatka Peninsula

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