A review of diatom δ18O in palaeoceanography

Swann, George E. A.; Leng, Melanie J.

doi:10.1016/j.quascirev.2008.11.002

Cited by 88 publications

(94 citation statements)

References 137 publications

(164 reference statements)

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“…During the global cooling event corresponding to MIS 2, mean summer water temperatures were obviously colder than during the MIS 3 and MIS 1 interstadials, inferred to be about 10-12 °C (Bezrukova et al, 2010;Müller et al, 2014). A 6-8°C water cooling leads to 1.2-1.6‰ δ 18 O enrichment, as estimated with regard to the oxygen isotope fractionation between biogenic silica and water corresponding to a temperature coefficient of -0.2‰/°C (Swann and Leng, 2009). The 1.8‰ difference in average δ 18 O diatom values between the warm and cold spells might be a consequence of water temperature change.…”

Section: Discussionmentioning

confidence: 93%

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Oxygen isotope composition of diatoms from sediments of Lake Kotokel (Buryatia)

Kostrova

Meyer

Tarasov³

et al. 2016

Russian Geology and Geophysics

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This is a summary of new oxygen isotope data for diatoms from Lake Kotokel sediments, with implications for responses of the lake system and its environment to global change over the past 46 kyr. Fossil diatoms in all samples are free from visible contamination signatures and contain no more than 2.5% Al 2 O 3 , which ensures reliable reconstructions. The δ 18 O values in diatoms vary between +23.7 and +31.2‰ over the record. The results mainly represent diatom assemblages of summer blooming periods, except for the time span between 36 and 32 kyr, when the isotopic signal rather records a shift from summer to spring blooming conditions. Possible water temperature changes only partly explain the changes in the isotopic record. The observed isotopic patterns are produced mainly by isotope changes in lake water in response to variations in air temperature, hydrology, and atmospheric circulation in the region. During Marine Isotope Stage (MIS) 2 (Last Glacial maximum), high δ 18 O diatom resulted from rapid evaporation and low fluvial inputs. The high δ 18 O values of about +29 to +30‰ during the first half of MIS 1 (Holocene interglacial) suggest an increased share of summer rainfalls associated with southern/southeastern air transport. The δ 18 O decrease to +24‰ during the second half of MIS 1 is due to the overall hemispheric cooling and increased moisture supply to the area by the Atlantic transport. The record of Lake Kotokel sediments provides an example of complex interplay among several climatic controls of δ 18 O diatom in the Late Pleistocene and the Holocene.

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Section: Discussionmentioning

confidence: 93%

“…Out of 142 specimens, only nine contained 2.6-4.9% Al 2 O 3 and 90.8-95.2% SiO 2 (Fig. 2) (Leng and Barker, 2006;Swann and Leng, 2009). The isotope record includes three distinct zones corresponding to the stages MIS 3-MIS 1 of marine oxygen stratigraphy (Fig.…”

Section: Methodsmentioning

confidence: 99%

Oxygen isotope composition of diatoms from sediments of Lake Kotokel (Buryatia)

Kostrova

Meyer

Tarasov³

et al. 2016

Russian Geology and Geophysics

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“…The measured oxygen isotope composition (δ 18 O measured ) was corrected (to δ 18 O corr ) using geochemical mass-balancing (Brewer et al, 2008; improved by Swann and Leng, 2009;Chapligin et al, 2012a). …”

Section: Contamination Assessment and Correctionmentioning

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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“…For δ 18 O diatom , a number of culture (Binz, 1987;Brandriss et al, 1998;Schmidt et al, 2001), sediment trap and down-core studies (Sancetta et al, 1985;Juillet-Leclerc and Labeyrie, 4/28 information for use in paleoenvironmental reconstructions (see Leng and Barker, 2006;Swann and Leng, 2009). …”

Section: Oxygen Isotopesmentioning

confidence: 99%

“…In the marine environment, δ 18 O diatom records can be used to investigate temperature and δ 18 O water variations in a manner which is similar to that used with δ 18 O records from foraminifera (δ 18 O foram ) (see Swann and Leng, 2009 (Shemesh et al, 1994;2002).…”

Section: Oxygen Isotopesmentioning

confidence: 99%