Deglaciation chronology of the Scandinavian Ice Sheet from the Lake Onega Basin to the Salpausselkä End Moraines

Saarnisto, Matti; Saarinen, Timo

doi:10.1016/s0921-8181(01)00131-x

Cited by 161 publications

(118 citation statements)

References 16 publications

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“…The same discrepancy is also observed in Sweden, where the varved clay chronology shows a considerably faster ice recession rate than other dating methods (Ringberg & Erlström, 1999). Calculated for the Pandivere Upland, the ice recession rate is comparable with that suggested for the Onega area (ca 200 m yr -1 ) (Saarnisto & Saarinen, 2001). However, the obtained AMS radiocarbon dates do not reflect the exact timing of the deglaciation, but rather the start of terrestrial vegetation colonisation.…”

Section: Timing Of the Deglaciation Of The Pandivere Uplandsupporting

confidence: 79%

“…This estimation is older than recently suggested (Kalm, 2012;Saarse et al, 2012;Lasberg & Kalm, 2013;Vassiljev & Saarse, 2013) and does not fit with 10 Be-based dates, which indicate that the Pandivere belt formed 13 100±1100 10 Be years BP (Rinterknecht et al, 2006). The varved clay results and their correlation with the Neva ice marginal belt (Saarnisto & Saarinen, 2001) provide grounds for estimating the age of the Pandivere stadial at 12 700 varve years (Hang, 1997), redefined to 13 300 varve years by Hang (2003) and later to more than 13 300 cal. yr BP (Hang & Kohv, 2013).…”

Section: Introductioncontrasting

confidence: 57%

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Timing of the deglaciation and the late-glacial vegetation development on the Pandivere Upland, North Estonia

Amon¹,

Saarse²,

Vassiljev³

et al. 2016

Bull Geol Soc Finland

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In this study, the deglaciation chronology of the Pandivere Upland is defined, and the late-glacial vegetation trends of north-eastern Estonia are summarised. The multi-proxy study includes accelerated mass spectrometry 14 C dating, plant macrofossil, magnetic susceptibility, loss-on-ignition and grain-size distribution data of the lacustrine sediment record from one previously unpublished study site (Kursi), and the study discusses the results in combination with five previously published study locations from the area.The results indicate that the deglaciation of the Pandivere Upland started at approximately 14 200 cal. yr BP and was completed by 13 800 cal. yr BP. The ice recession rate was approximately 180 m yr -1 . Based on these new radiocarbon dates, the Baltic Ice Lake stage A 1 submerged the northern and western ice-free areas of Estonia by ca. 13 800 cal. yr BP. The prevalent vegetation type in north-eastern Estonia during the late-glacial period was tundra with local variations in the dominant shrub species. The region remained treeless until the Holocene.

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Section: Timing Of the Deglaciation Of The Pandivere Uplandsupporting

confidence: 79%

Section: Introductioncontrasting

confidence: 57%

Timing of the deglaciation and the late-glacial vegetation development on the Pandivere Upland, North Estonia

Amon¹,

Saarse²,

Vassiljev³

et al. 2016

Bull Geol Soc Finland

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“…13,900-13,800 cal yr BP (Hang et al, 2011). These ages are 300-500 years older than those sug gested earlier (Vassiljev et al, 2005;Saarse et al, 2007;Rosentau et al, 2009) based on data from the Karelian Isth mus (Wohlfarth et al 1999;Saarnisto and Saarinen, 2001), as AMS dates from the Es to nian sites were not avail able at that time. The ice reces sion could have oc curred even ear lier, as lac us trine sed imen ta tion in front of the re ced ing gla cier may have been delayed by a few hun dred years (Warner et al, 1991).…”

Section: Chronology Of Deglaciation -Discussionmentioning

confidence: 60%

Deglaciation chronology of the Pandivere and Palivere ice-marginal zones in Estonia

Saarse¹,

Heinsalu²,

Veski³

2012

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Ac cel er a tor mass spec trom e try (AMS) 14 C dates, pol len and plant macrofossil ev i dence and lithostratigraphic pa ram e ters ob tained from four Late Gla cial lake sed i ment re cords were used to study the deglaciation chro nol ogy of Es to nia. AMS dates show that the north ern part of the Saadjärv Drum lin Field was free of ice cover at ap prox i mately 14,300-14,200 cal yr BP. These ages fit well with the ice re treat es tima tions (14,700-14,500 cal yr BP) of the Otepää ice-mar ginal zone in the south and the deglaciation of the Pandivere Up land in the north (13,800 cal yr BP). Glaciolacustrine sed i ments of the Haljala and Udriku bas ins were de pos ited in proglacial lake A 1 , a north east ern bay of the Bal tic Ice Lake that al ready ex isted ca. 13,800 cal yr BP. The Palivere ice-mar ginal zone, and proglacial lake A 2 as so ci ated with it, was formed ca. 500 years later, at ap prox i mately 13,200 cal yr BP. New ev i dence in di cates that ice re advance dur ing the Palivere stade ter mi nated dur ing the AllerÝd chronozone.Leili Saarse, Atko Heinsalu and Siim Veski, In sti tute of Ge ol ogy at Tallinn Uni ver sity of Tech nol ogy, Ehitajate tee 5, 19086 Tallinn, Esto nia;

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“…This chronological relation of the Saint-Narcisse morainic complex and later moraines with Younger Dryas, based on current data in Canada, remind us of the chronology of the Salpausselkä Moraines in Finland. According to Sauramo (1929), Rainio (1995), Saarnisto and Saarinen (2001), and Rinterknecht et al (2004), the Salpausselkä Moraines were formed along the southern margin of the Scandinavian Ice Sheet during several episodes of Younger Dryas: a readvance of about 80 km in less than 700 varve-years, the Salpausselkä Moraine I deposition for 217 varve-years, a 40 km margin retreat for 200 varve-years, and the deposition of the Salpausselkä Moraine II for 183 varve-years. Due to the lack of solid ages on the southern margin of the LIS, it is too early to propose a direct correlation of the Saint-Narcisse Moraine with the Younger Dryas moraines of Finland and the rest of Scandinavia.…”

Section: Relation Of the Saint-narcisse Morainic Complex With Youngermentioning

confidence: 99%

The Saint-Narcisse morainic complex and early Younger Dryas events on the southeastern margin of the Laurentide Ice Sheet

Occhietti

2010

gpq

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The Saint-Narcisse morainic complex extends over 750 km along the southern margin of the Laurentian Highlands in Québec, north of the St. Lawrence Valley, between the Ottawa and Saguenay Rivers. To the east, the Laurentide Ice Sheet margin was located in the present St. Lawrence Estuary. To the west, the morainic complex is extended 235 km west of the Ottawa River to the Algonquin Highlands, in Ontario. The general outline of the morainic complex comprises large lobes and reentrants, related to major topographic features. In the lower Saint-Maurice River area, the moraine is composed of reworked clay and till and proximal glaciomarine deposits (Yamachiche Diamicton) and melt-out till and ice-marginal outwash (Charette Drift). The Saint-Narcisse Event can be subdivided in several phases: local readvance in low areas, main phase at the origin of the Saint-Narcisse Moraine s.s., melting-out of the marginal ice with compressive structures and large proglacial outwash features, and slow retreat with secondary ridges. The accuracy of the chronological data is limited by several factors: and a floating chronology is proposed. Two landmarks constrain the age and range of duration of the main Saint-Narcisse phase. The main ridge deposition occured after the onset, ca. 12.9 cal ka, of Champlain Sea in the St. Lawrence Valley, and a rapid ice retreat on the southern edge of the Laurentians. It ended before the drawdowm, in the Lake Huron basin, of Glacial Lake Algonquin ca. 12.5 cal ka. The Saint-Narcisse Event is related to the early cold phase of Younger Dryas, as evidenced by other YD ice readvances in Maine, Nova Scotia, and ice cover on the Gaspé Peninsula. It corresponds to a positive change of the budget of the Laurentide Ice Sheet as a result of climate forcing. After a slow ice front retreat during about 900-700 yr, the final phase of YD is marked by the Mars-Batiscan Moraine, located 17 to 70 km north of the Saint-Narcisse Moraine.Le complexe morainique de Saint-Narcisse s’étend sur 750 km le long de la marge méridionale des Laurentides, au Québec, au nord de la vallée du Saint-Laurent, entre l’Outaouais et le Saguenay. Vers l’est, la marge glaciaire était située dans l’estuaire actuel du Saint-Laurent. Vers l’ouest, en Ontario, les formes associées sont suivies dans le massif Algonquin, jusqu’à 235 km de l’Outaouais. Le tracé général du complexe inclut de grands lobes et rentrants liés à la topographie. Dans la basse vallée du Saint-Maurice, la Moraine de Saint-Narcisse est composée de dépôts glaciomarins proximaux, de till et d’argile marine remaniée (Diamicton de Yamachiche) et de till de fusion sur place et de dépôts fluvioglaciaires et juxtaglaciaires (Dépôts de Charette). L’Épisode de Saint-Narcisse est subdivisé en plusieurs phases non nécessairement synchrones sur toute la marge glaciaire: réavancée locale dans les dépressions importantes, phase majeure de stabilisation à l’origine de la Moraine de Saint-Narcisse, fonte sur place indiquée par des structures imbriquées et épandages proglaciaires, puis retra...

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Deglaciation chronology of the Scandinavian Ice Sheet from the Lake Onega Basin to the Salpausselkä End Moraines

Cited by 161 publications

References 16 publications

Timing of the deglaciation and the late-glacial vegetation development on the Pandivere Upland, North Estonia

Timing of the deglaciation and the late-glacial vegetation development on the Pandivere Upland, North Estonia

Deglaciation chronology of the Pandivere and Palivere ice-marginal zones in Estonia

The Saint-Narcisse morainic complex and early Younger Dryas events on the southeastern margin of the Laurentide Ice Sheet

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