Ice-free interval corresponding to Marine Isotope Stages 4 and 3 at the Last Glacial Maximum position at Kileshino, Valdaj Upland, Russia/MIS 4-3 jaavabad intervallid viimase jaatumise maksimumlevikupiiril Kilesinos Valdai korgustikul Venemaal.
The extent and timing of the Scandinavian Ice Sheet (SIS) during the Valdaj (also spelt Valdai or Valday) (Weichselian) cold stages have been investigated previously by many authors. In the NW part of European Russia, however, especially in the area of Valdaj, the chronological data are still insufficient and further studies are required.
Contradictory opinions exist regarding the advance of the SIS to the NW part of European Russia during the Valdaj cold stage. Some studies claim that the area was covered by the SIS twice: (1) in the early or middle (Marine Isotope Stage (MIS) 4), and (2) the late Valdaj (Zarrina 1991; Arslanov 1993). Other studies, however, state that the SIS advanced to the NW part of European Russia only during the late Valdaj, while in the early/middle Valdaj the margin of the SIS did not reach beyond the Baltic Sea Depression and Russian Karelia (Chebotareva & Makarycheva 1982; Velichko et al. 2004, 2011). The extent and timing of the SIS during the Last Glacial Maximum (LGM) in different areas have been estimated by many authors (Larsen et al. 1999; Lunkka et al. 2001; Rinterknecht et al. 2007, 2008; Wysota et al. 2009; Marks 2010; Guobyte & Satkunas 2011; Lasberg & Kalm 2013). Yet, the timing of the LGM has not been suggested in the region close to the Valdaj Upland and the extent of the LGM has been modelled based on glacial landforms and geomorphology (Ehlers & Gibbard 2004; Kalm 2012). Thus, it is essential to have more chronological proof to confirm the modelled position.
Previously, several authors (Vigdorchik et al. 1974; Zubakov 1974; Malakhovskij & Spiridonova 1981; Arslanov 1987) have published radiocarbon dates from the Kileshino site in the Valdaj Upland. Chronological data together with sedimentology have been summarized by Zarrina (1991) and palynological analysis has been made by Giterman et al. (1975).
The aim of the current study is to define ice-free intervals in the Kileshino outcrop based on bio- and lithostratigraphical data, radiocarbon and optically stimulated luminescence (OSL) dates and to interpret the timing of glacial sediments found from the outcrop. In addition, we intend to check the interpretations based only on palynological data (Giterman et al. 1975) using modern dating methods.
The study site is located in the central part of the Valdaj Upland (western part of the Russian Plain), on the East European Platform in the Tver region of Russia. The outcrop of Kileshino (56.88033[degrees]N, 33.45834[degrees]E) is located near Kileshino village on the left bank of the Sizhina River, ca 4 km north of the town of Selizharovo and 10 km east of Lake Volgo (Fig. 1). The area around the outcrop is plain and several 1 m high boulders are found in the surroundings. The study site (~ 215 m a.s.l.) lies close to the margin of the modelled last SIS during its maximum extent (Kalm 2012). The Valdaj Upland area is generally a slightly hilly plain with average elevations from 150 to 250 m a.s.l. and the highest point of 346.9 m a.s.l. near the town of Vyshnij Volochek. The southern part of the Valdaj Upland appears to be the main watershed between the drainages of the Caspian and Baltic seas on the East European Platform.
MATERIAL AND METHODS
Field work and sampling were performed at the Kileshino outcrop in the autumn of 2011. The outcrop was described, sampled and photographed in the field. Detailed sedimentological studies were carried out and five main sedimentary units and 19 lithofacies were distinguished. The lithofacies classification used in Fig. 2 is modified from Eyles et al. (1983) and Kruger & Kjsr (1999); sediment colour was identified according to Munsell's colour system chart (Munsell Color 1998).
Samples for dating were taken below the till for determining the age of the last SIS advance and the ages of sedimentary units. Four samples for OSL dating of fluvial and limnic sediments from depths of 268-258, 231-158, 141-111 and 80-78 cm (Fig. 2) were collected in plastic tubes and sent to the Laboratory of Chronology, University of Helsinki, for age estimation. The samples were measured by the Rise TL-DA-12 reader and equivalent doses were estimated using a single-aliquot regenerative-dose protocol (Murray & Wintle 2000). Six samples for radiocarbon dating by the accelerator mass spectrometry (AMS) method were taken from depths of 545, 375-365, 355-350, 310-295, 273-268 and 258-252 cm (Fig. 2) and examined in detail in order to define terrestrial and aquatic plant macrofossils for each sample before dating. The main purpose of this determination was to minimize the age overestimations, because the aquatic macrofossils have a 'reservoir effect' compared to macrofossils of terrestrial origin (Hua 2009), but also some general conclusions about climate were made based on the identified species. Samples for macrofossil analyses were washed under tap water through a sieve with a 0.25 mm mesh. Plant remains were picked out under an Olympus SZ61 stereomicroscope. Identification was done under a Nikon SMZ800 low-power stereomicroscope using the keys of Katz et al. (1965, 1977) and Schoch et al. (1988) and the reference collection of seeds and fruits of the Laboratory of Geoarchaeology and Ancient Technology at the Institute of History in Tallinn.
The AMS ages were determined in the Beta Analytic Radiocarbon Dating Laboratory, Florida, USA. The dates were calibrated with 1o uncertainty using the IntCal09 calibration curve (Reimer et al. 2009) and the OxCal v.4.1 program (Bronk Ramsey 2009).
RESULTS AND INTERPRETATIONS
The outcrop opens up 545 cm of sediments. Based on sediment lithology and dating, five main sedimentary units were determined (Fig. 2).
Sedimentary unit 1 (SU1) comprises two layers of laminated silt and sand. The bottommost layer (545469 cm) is fine-layered laminated silt and sand (colour 10YR/4/2--dark greyish-brown) containing some finely disseminated organic layers. It is overlain by a layer of sediments of the same type (469-379 cm) but different colour (2.5YR/5/2--weak red). At a depth of 399-379 cm the sediments are massive, not stratified. Sediments of SU1 refer to rhythmic deposition of varved clay under periglacial conditions. One [sup.14]C AMS sample was taken from the bottommost section of this unit.
Sedimentary unit 2 (SU2) has a transitional basal contact with SU1. The bottommost layer (379-273 cm) is fine-layered silt with gyttja and plant macrofossils (7.5YR/3/1--very dark grey). The upper part of SU2 consists of three thin layers: a layer of compressed, finely laminated peat with silt (273-268 cm; 10YR/2/1--black) interchanges to laminated fine sand with a diffused peat layer (268-258 cm; 10YR/5/3--brown) and to a well-decomposed peat layer (2.5YR/2.5/2--very dusky red) at a depth of 258-252 cm. All three topmost layers of SU2 have transitional lower and upper bedding surfaces. The unit SU2 indicates the change in sedimentation conditions, as rhythmic flood-plain sediments in the lower part change to typical limnic sediments in the upper part. Altogether, six [sup.14]C AMS samples were taken from the lower, central and top parts of this unit.
Sedimentary unit 3 (SU3) shows rhythmic sedimentation--laminated silt and sand layers typical of fluvial sedimentation systems interchange throughout the unit. The 252-231 cm interval of stratified brown (7.5YR/5/2; 7.5YR/4/2) silt and sand is overlain by sediments of the same type but of different colour (5YR/3/3--dark reddish-brown to 10YR/5/4--yellowish-brown) with some organic layers inside (231-158 cm). The next layer (158-141 cm) is massive, reddish-grey (5YR/5/2) silt with diffused organics, overlain by an interval (141-111 cm) of varicoloured (5YR/4/4--reddish-brown and 10YR/6/4--light yellowish-brown), deformed and stratified silt and medium sand. The layer at a depth of 111-91 cm is greyish-brown (10YR/4/2--dark greyishbrown in the lower part; 10YR/5/2--greyish-brown in the upper part), massive and blockish silt containing some gravel. It is covered by a dark yellowish-brown (10YR/4/6), massive silt layer (91-80 cm) overlain by a thin layer of light brownish-grey (10YR/6/2), loose and massive fine sand (80-78 cm). Layers in SU3 are contorted and their bedding planes are mostly wavy, which indicates that they were deformed after deposition.
Sedimentary unit 4 (SU4) comprises a layer of greyish-brown (10YR/5/2) loam with pebbles up to 5 cm in diameter at a depth of 78-40 cm, overlain (40-23 cm) by brown (10YR/5/4--yellowish-brown to 5YR/4/4--reddish-brown), loose and stratified sand with gravel in its lower part. The unit SU4 refers to a glacial environment as it comprises sediments of different grain sizes from silt to pebbles (till) and gravel without apparent organics.
The topmost sedimentary unit (SU5) from the interval 23-0 cm is brownish silty soil.
Ages and climate-chronological interpretations of sedimentary units
Climate-chronological interpretations for all sedimentary units were made based on four OSL and six [sup.14]C AMS age estimations from different depths (Tables 1 and 2) and identified plant macrofossils (Table 3).
It was possible to obtain only one infinite AMS [sup.14]C age from SU1 (Fig. 2). The terrestrial macrofossil (Betula alba) was estimated to be older than 43.5 14C ka BP, which is close to the maximum age that can be determined by the radiocarbon dating method. Based on one radiocarbon date (> 43.5 [sup.14]C ka BP), we assume that SU1 was deposited before the late Valdaj and not later than 43.5 [sup.14]C ka BP. Furthermore, the genesis of the sediments (varved clay) indicates cold conditions typical of late glacial periods and ages from the sedimentary unit above (SU2) show that the study site was ice-free during MIS 3. We concluded that SU1 was deposited in the peripheral zone of the SIS margin earlier than MIS 3.
Four AMS [sup.14]C dates from SU2 yielded the age of > 43.5 [sup.14]C ka BP for terrestrial and aquatic macrofossils (Table 1, Fig. 2). Three AMS dates of terrestrial macrofossils were between 33.8 and 44.8 cal [sup.14]C ka BP. Also one OSL age, 57.5 [+ or -] 12.9 ka, was determined from that unit (Table 2, Fig. 2). Thus, the ages from SU2 vary from 57.5 OSL to 33.8 cal [sup.14]C ka BP. Some identified plant macrofossils (Betula alba, Betula pubescens, Populus tremula, Salix sp.) are cold-tolerating species that are native and abundant throughout northern Europe and indicate that during SU2 the climate was similar to the nowadays one, which implies ice-free conditions (Table 3). Plant macrofossils (Najas marina, Carex vesicaria, Schoenoplectus lacustris, Nuphar lutea) that typically inhabit wet areas like lakes, ponds and swamps were also found from SU2. Furthermore, Najas marina, Schoenoplectus lacustris and Nuphar lutea from the upper part of SU2 indicate that the water level was lowering.
Based on dates, identified plant macrofossils and the genesis of sediments, SU2 corresponds to the middle Valdaj (MIS 3) 'megainterstadial' in European Russia (from Oerel to Hengelo interstadials in Central Europe) (Arslanov 1993; Velichko et al. 2011). The MIS 3 'megainterstadial' is characterized by alternating warm and cool phases and, based on the age interval of SU2, the sediments from the Krasnogorskij interstadial (OerelGlinde interstadials in Central Europe) to the Leningradskij interstadial (Moershoofd-Hengelo interstadials in Central Europe) are present (Velichko et al. 2011).
Three OSL ages determined from SU3 resulted in inconsistent ages compared to SU2 (Table 2, Fig. 2). The unit SU3 should be younger than the unit below according to the superposition principle, but OSL samples yielded the ages of 72.2 [+ or -] 12.9, 69.6 [+ or -] 12.7 and 40.8 [+ or -] 6.9, which are older than the ages from SU2. Unfortunately there was no material for [sup.14]C AMS dating of SU2 for age comparisons. Because dates from SU3 are inconsistent with other ages below and considering also the fact that layers are contorted, we have a reason to conclude that the whole unit was replaced and moved to the Kileshino site by the last SIS advance. The sediments of SU3 are fluvial in origin and, based on the dates from SU3, we suggest that the lower part of SU3 corresponds to the middle Valdaj Shestikhino stadial (Schalkholz stadial in Central Europe) and the upper part to the middle Valdaj Leningradskij interstadial in European Russia (Moershoofd-Hengelo interstadials in Central Europe) (Velichko et al. 2011). No dates from SU4 or above are available, and thus the age of till found from SU4 is not older than 33.8 cal 14C ka BP, which is the youngest age estimated from the organics in rhythmic flood-plain sediments under till and sands, and corresponds to the late Valdaj glaciation.
To sum up, the age range of 72.2 OSL to 33.8 cal [sup.14]C ka BP obtained from our outcrop shows that the SIS did not reach the Kileshino site during MIS 4 between 72.2 and 58 OSL ka. Yet, there is no chronological information about the time between 115 and 72.2 OSL ka in our outcrop.
Radiocarbon dates taken below till at the Kileshino site ranged between > 43.5 and 33.8 cal 14C ka BP, indicating the existence of ice-free conditions. Previously, several wood samples have been dated by the radiocarbon dating method that yielded ages between 53.5 OSL and 43.2 cal [sup.14]C ka BP (Arslanov 1987), which also supports our findings. However, there is a contradiction in regard to the lithology when comparing our results with previous work. We have interpreted the one till present at Kileshino to be late Valdaj in age, while Zarrina (1991) considered it to be of middle Valdaj age. A possible explanation could be that there are two tills present at the Kileshino site and Zarrina (1991) refers to the lower till, while the description of the upper part of the outcrop between middle Valdaj till and soil is absent. Nevertheless, the discrepancy between our data and the age of the lower till remains. This can be explained by misinterpretation of this sediment, which could actually be some other sediment. Also Zarrina (1991) doubted the glacial origin of the sedimentary unit interpreted as till, because she described it as 'atypical facies variations' of till (clayey with some boulders). Data from the areas adjacent to the study site (Arkhangelsk region, Karelia and Vologda area) support the idea that the uppermost till found at the Kileshino site is late Valdaj in age. None of the outcrop sections or boreholes of that region contain early Valdaj till of SIS origin (Demidov et al. 2004) and recent studies as well claim that during the Valdaj glaciation the study area was overridden by the SIS only once, in the late Valdaj (Velichko et al. 2004, 2011).
Sedimentary unit 1 (SU1) at our study site was possibly deposited in the periglacial area and on the basis of our chronological data, earlier than MIS 3, while the SIS did not override the Kileshino site. Supposing that a middle (MIS 4) Valdaj glaciation occurred in European Russia as some authors have suggested, and SU1 was deposited at that time, no hiatus existed in the outcrop between SU1 and SU2. The reason is that during the MIS 3 'megainterstadial' in European Russia (Oerel to Moershoofd interstadials in Central Europe) the water level of the ice-dammed lake in front of the SIS margin dropped and SU2 was formed as the lake changed to a typical non-glacial shallow lake and the deposition of peat started. But if SU1 is considered to be older than MIS 4 (coeval with MIS 6 Moscow stage in European Russia; late Saalian in Central Europe), sediments of MIS 5e Mikulino interglacial in European Russia (Eemian interglacial in Central Europe) are absent from the Kileshino outcrop. This contradicts the results of Giterman et al. (1975) who, on the basis of palynological analysis, assigned the sediments under peat at the Kileshino site to the Mikulino interglacial. However, no chronological data were available at that time to prove it. Our radiocarbon and OSL dates do not support this conclusion as SU2 is younger than the Mikulino interglacial and SU1 is described as periglacial sediments.
Sedimentary unit 3 (SU3) presumably redeposited at the Kileshino site in the course of the advance of late Valdaj glaciers, since a fast-flowing NW-SE directed ice-stream corridor existed in that area (Demidov et al. 2006). Nevertheless, dates from SU3 (if they are reliable) still exhibit an ice-free time at Kileshino during MIS 4 and 3 at the same time as the area to the NW of Kileshino was ice-free, relying on the fact that the general direction of the last SIS advance was from NW to SE. The upper part of SU3 could refer to the 'atypical till' described by Zarrina (1991), because her description of the lithology together with the dates is similar to our data.
Sedimentary unit 4 (SU4), which represents late Valdaj till, could have been deposited by debris ice. It has been assumed that the long and thin lobes of fastflowing ice streams between the Gulf of Finland and the LGM position in the study area became detached from the SIS during deglaciation (Demidov et al. 2006). Unfortunately, the late Valdaj age has not been dated directly and based on our dates from the outcrop, it can only be concluded that the last SIS reached the Kileshino site not before 33.8 cal [sup.14]C ka BP. Previous works suggest that the SIS reached its maximum position in the Vologda area at 18 OSL ka (Lunkka et al. 2001), in Russian Karelia not before 17 OSL ka (Larsen et al. 1999) and in NE Belarus not before 19.1 cal [sup.14]C BP (Zimenkov 1989). Thus, the last SIS reached the Kileshino site presumably between ca 19.1 cal [sup.14]C BP and 18 OSL ka. This corresponds well with 20-18 ka, which has also been suggested as the LGM age in NW Russia (Demidov et al. 2006).
--According to our chronological data, the SIS reached the Kileshino site only once during the last 72.2 OSL ka in the late Valdaj, after 33.8 cal [sup.14]C ka BP and presumably between 19.1 cal vC BP and 18 OSL ka.
--Based on the dated sediments, limnic sedimentation conditions existed at the Kileshino site during MIS 3, between 57.5 OSL and 33.8 cal [sup.14]C ka BP, which corresponds to the middle Valdaj 'megainterstadial' in European Russia (Oerel to Hengelo interstadials in Central Europe).
--To the NW of Kileshino, fluvial sedimentation conditions occurred during 72.2-40.8 OSL ka on the basis of our chronological data.
--According to our interpretation that SU3 was redeposited by the advancing SIS at the Kileshino site and together with available dates from SU2, which express the ages in situ, we conclude that ice-free conditions existed during 72.2 OSL-33.8 cal [sup.14]C ka BP at that site.
Kaesoleva uuringu tulemused naitavad, et ajavahemikul 72 200-33 800 kalendriaastat tagasi, mis vastab neljandale ja kolmandale merelisele isotoopstaadiumile (MIS 4 ning MIS 3), oli viimase Skandinaavia jaatumise maksimumlevikupiiril olev Kilesino jaavaba. Dateeringutest ilmnevad jarvelised sedimentatsioonitingimused Kilesinos ajavahemikul 57 500-33 800 kalendriaastat tagasi, mis vastab MIS 3 megainterstadiaalile Venemaa Euroopa-osas (Oereli kuni Hengelo interstadiaal Kesk-Euroopas). Skandinaavia mandriliustik kandis oma viimasel pealetungil Kilesinosse vooluveelise settekompleksi, mille moodustavad vaheldumisi aleuriidi- ja liivakihid. Settekompleks ise valjendab vooluveelisi settetingimusi Kilesinost loode pool ajavahemikul 72 200-40 800 aastat tagasi. Koiki dateeringuid arvesse vottes jareldub, et Kilesino oli viimase Skandinaavia jaatumise ajal jaavaba ajavahemikul 72 200-33 800 kalendriaastat tagasi ja aleuriidi-liivakihtidega settekompleks transporditi uuringualale hiljem kui 33 800 kalendriaastat tagasi, lahtudes aga varasematest toodest toenaoliselt liustiku maksimumlevikul ajavahemikul umbes 19 100-18 000 aastat tagasi. Kilesinost leiti ainult uks noorem kui 72 200 aastat vana moreenkiht ja sellest jareldub, et Skandinaavia mandriliustik joudis uuringualale ainult uhe korra viimase 72 200 aasta jooksul: HilisValdais (Weichsel) hiljem kui 33 800 kalendriaastat tagasi. Skandinaavia mandriliustiku laienemine uuringualale ajavahemikul 115 000-58 000 aastat tagasi ei leidnud kinnitust ega umberlukkamist, kuna ajavahemiku 115 000 kuni 72 200 aastat tagasi kohta puuduvad kronoloogilised andmed.
Received 9 September 2013, accepted 31 December 2013
Acknowledgements. This study was funded by the Estonian Research Council (project SF0180048s08, grants 7563 and 9107). K. Sohar, T. Hang and A. Gorlach are thanked for assistance with field work and S. Hiie is appreciated for help in identifying plant macrofossils. We thank Proof-ReadingServices.org for profound language corrections. We are grateful to A. Molodkov, A. A. Velichko and J. Satktmas for their suggestions and constructive criticism for improving the manuscript.
Arslanov, Kh. A. 1987. Radiouglerod: geokhimiya i geokhronologiya [Radiocarbon: Geochemistry and Geochronology]. University of Leningrad, Leningrad, 300 pp. [in Russian].
Arslanov, Kh. A. 1993. Late Pleistocene geochronology of European Russia. Radiocarbon, 35, 421-427.
Bronk Ramsey, C. 2009. Bayesian analysis of radiocarbon dates. Radiocarbon, 51, 337-360.
Chebotareva, N. S. & Makarycheva, I. A. 1982. Geochronology of environmental evolution within the glaciated area of Eastern Europe during the Valday epoch. In Paleogeografiya Evropy za poslednie sto tysyach let [Paleogeography of Europe in the Last 100,000 Years] (Gerasimov, I. P. & Velichko, A. A., eds), pp. 36-48. Nauka, Moscow [in Russian].
Demidov, I. N., Houmark-Nielsen, M., Kjasr, K. H., Larsen, E., Lysa, A., Funder, S., Lunkka, J. P. & Saarnisto, M. 2004.
Valdaian glacial maxima in Arkhangelsk district of northwestern Russia. In Quaternary Glaciations: Extent and Chronology, Part I: Europe (Ehlers, J. & Gibbard, P. L., eds), pp. 321-335. Elsevier, Amsterdam.
Demidov, I. N., Houmark-Nielsen, M., Kjasr, K. H. & Larsen, E. 2006. The last Scandinavian Ice Sheet in northwestern Russia: ice flow patterns and decay dynamics. Boreas, 35, 425-443.
Ehlers, J. & Gibbard, P. L. 2004. Quaternary Glaciations Extent and Chronology: Europe, Part I. Elsevier, Amsterdam, 475 pp.
Eyles, N., Eyles, C. H. & Miall, A. D. 1983. Lithofacies types and vertical profile models; an alternative approach to the description and environmental interpretation of glacial diamict and diamictite sequences. Sedimentology, 30, 395-410.
Giterman, R. E., Kuprina, N. P. & Zhantser, E. V. 1975. O mikulinskom vozraste mezhlednikovykh sloev u d. Kileshino (verkhnyaya Volga) [About Mikulino interglacial sediment layers near the Kileshino village (Upper Volga)]. Bulletin of Commission for Quaternary Research, 44, 84-89 [in Russian].
Guobyte, R. & Satkunas, J. 2011. Pleistocene glaciations in Lithuania. In Developments in Quaternary Science 15 (Ehlers, J., Gibbard, P. L. & Hughes, P. D., eds), pp. 231246. Elsevier, Amsterdam.
Hua, Q. 2009. Radiocarbon: a chronological tool for the recent past. Quaternary Geochronology, 4, 378-390.
Kalm, V. 2012. Ice-flow pattern and extent of the last Scandinavian Ice Sheet southeast of the Baltic Sea. Quaternary Science Reviews, 44, 51-59.
Katz, N. Y., Katz, S. V. & Kipiani, M. G. 1965. Atlas i opredelitel plodov i semyan vstrechayushchikhsya v chetvertichnykh otlozheniyakh SSSR [Atlas and Keys of Fruits and Seeds Occurring in the Quaternary Deposits of the U.S.S.R.]. Nauka, Moscow, 366 pp. [in Russian].
Katz, N. Y., Katz, S. V. & Skobeeva, E. I. 1977. Atlas rastitel nykh ostatkov v torfakh [Atlas of Plant Remains in Peat]. Nedra, Moscow, 372 pp. [in Russian].
Kruger, J. & Kjasr, K. H. 1999. A data for field description and genetic interpretation of glacial diamict and associated sediments - with examples from Greenland, Iceland and Denmark. Boreas, 28, 3 86-402.
Larsen, E., Lysa, A., Demidov, I., Funder, S., HoumarkNielsen, M., Kjasr, K. H. & Murray, A. S. 1999. Age and extent of the Scandinavian ice sheet in northwest Russia. Boreas, 28, 115-132.
Lasberg, K. & Kalm, V. 2013. Chronology of Late Weichselian glaciation in the western part of the East European Plain. Boreas, 42, 995-1007.
Lunkka, J. P., Saarnisto, M., Gey, V. & Demidov, I. 2001. Extent and age of the Last Glacial Maximum in the southeastern sector of the Scandinavian Ice Sheet. Global and Planetary Change, 31, 407-425.
Malakhovskij, D. B. & Spiridonova, A. E. 1981. O nizhnevaldajskikh otlozheniyakh nekotorykh voprosakh palaeogeografii poslednego oledeneniya Severo-Zapada Russkoj ravniny [About Early-Valday deposits and some questions about palaeogeography of the last glaciation in the northwest of the East European Plain]. In Geologiya plejstotsena Severo-Zapada SSSR. Apatity [Pleistocene Geology of NW of European USSR. Apatity] (Evzerov, V. Ya., ed.), pp. 62-71. Academy of Sciences of the USSR, Kola [in Russian].
Marks, L. 2010. Timing of the Late Vistualian (Weichselian) glacial phases in Poland. Quaternary Science Reviews, 44, 81-88.
Munsell Color. 1998. Munsell Soil Color Charts, Revised Washable Edition. GretagMacbeth, New Windsor, NY.
Murray, A. & Wintle, A. 2000. Luminescence dating of quartz using an improved single-aliquot regenerative-dose protocol. Radiation Measurements, 32, 57-73.
Reimer, P. J., Baillie, M. G. L., Bard, E., Bayliss, A., Beck, J. W., Blackwell, P. G., Bronk Ramsey, C., Buck, C. E., Burr, G. S., Edwards, R. L., Friedrich, M., Grootes, P. M., Guilderson, T. P., Hajdas, I., Heaton, T. J., Hogg, A. G., Hughen, K. A., Kaiser, K. F., Kromer, B., McCormac, F. G., Manning, S. W., Reimer, R. W., Richards, D. A., Southon, J. R., Talamo, S., Turney, C. S. M., van der Plicht, J. & Weyhenmeyer, C. E. 2009. IntCal09 and Marine09 radiocarbon age calibration curves, 0-50,000 years cal BP. Radiocarbon, 51(4), 1111-1150.
Rinterknecht, V. R., Pavlovskaya, I. E., Clark, P. U., Raisbeck, G., Yiou, F. & Brook, E. J. 2007. Timing of the last deglaciation in Belarus. Boreas, 36, 307-313.
Rinterknecht, V. R., Bitinas, A., Clark, P. U., Raisbeck, G. M., Yiou, F. & Brook, E. J. 2008. Timing of the last deglaciation in Lithuania. Boreas, 37, 426-433.
Schoch, W. H., Pawlik, B. & Schweingruber, F. H. 1988. Botanische makroreste. P. Haupt, Bern & Stuttgart, 205 pp.
Velichko, A. A., Faustova, M. A., Gribchenko, Yu. N., Pisareva, V. V. & Sudakova, N. G. 2004. Glaciations of the East European Plain--distribution and chronology. In Quaternary Glaciations--Extent and Chronology, Part I: Europe (Ehlers, J. & Gibbard, P. L., eds), pp. 337-354. Elsevier, Amsterdam.
Velichko, A. A., Faustova, M. A., Pisareva, V. V., Gribchenko, Yu. N., Sudakova, N. G. & Lavrentiev, N. V. 2011. Glaciations of the East European Plain: distribution and chronology. In Developments in Quaternary Science 15 (Ehlers, J., Gibbard, P. L. & Hughes, P. D., eds), pp. 337-359. Elsevier, Amsterdam.
Vigdorchik, M., Zarrina, E., Krasnov, I. & Auslender, V. 1974. Late Pleistocene. In Geokhronologiya SSSR 3. Novejshij etap [Geochronology of the USSR 3, The Latest Phase] (Zubakov, V. A., ed.), pp. 55-75. Nedra, Leningrad [in Russian].
Wysota, W., Molewski, P. & Sokolowski, R. J. 2009. Record of Vistula ice lobe advances in the Late Weichselian glacial sequence in north-central Poland. Quaternary International, 207(1-2), 26-41.
Zarrina, E. P. 1991. Chetvertichnye otlozheniya severo-zapadnykh i tsentral 'nykh rajonov Evropejskoj chasti SSSR [Quaternary Deposits of the Northwest and Central Regions of the European Part of the USSR]. Nedra, USSR Ministry of Geology, Leningrad, 127 pp. [in Russian].
Zimenkov, O. I. 1989. Vremya kulminatsii poozerskogo oledeneniya na territorii Belorusii [The timing of the Poozerian Glaciation maximum in the territory of Belarus]. In Novoe v izuchenii kainozojskikh otlozhenij Belorusii i smezhnykh oblastej [New in the Study of Cenozoic Sediments of Belarus and Adjacent Regions] (Matveev, A. V., ed.), pp. 30-45. Nauka i tekhnika, Minsk [in Russian].
Zubakov, V. A. 1974. Pozdnij pliotsen--chetvertichnyj period [Late Pliocene--Quaternary]. In Geokhronologiya SSSR 3. Novejshij etap [Geochronology of the USSR 3, The Latest Phase] (Zubakov, V. A., ed.), pp. 44-84. Nedra, Leningrad [in Russian].
Katrin Lasberg, Volli Kalm and Kersti Kihno
Institute of Ecology and Earth Sciences, University of Tartu, Ravila 14a, 50411 Tartu, Estonia; email@example.com
Received 9 September 2013, accepted 31 December 2013
Table 1. [sup.14]C ages Lab. No. Sample No. Depth, [sup.14]C BP, cm ka Beta-315232 KIL-1 258-252 41.11 [+ or -] 0.42 Beta-315234 KIL-2 273-268 > 43.5 Beta-315236 KIL-3 310-295 > 43.5 Beta-315237 KIL-3-2 310-295 > 43.5 Beta-315238 KIL-4 355-350 37.85 [+ or -] 0.33 Beta-315239 KIL-4-2 355-350 > 43.5 Beta-315240 KIL-5 375-365 29.12 [+ or -] 0.17 Beta-315241 KIL-6 545 > 43.5 Lab. No. Cal [sup.14]C BP Median of Origin of plant (1[sigma]), cal age, macrofossils ka ka Beta-315232 44.46-45.12 44.8 Terrestrial Beta-315234 -- -- Terrestrial Beta-315236 -- -- Terrestrial Beta-315237 -- -- Aquatic Beta-315238 42.15-42.69 42.4 Terrestrial Beta-315239 -- -- Aquatic Beta-315240 33.38-34.41 33.8 Terrestrial Beta-315241 -- -- Terrestrial Table 2. OSL ages Lab. No. Sample Depth, Dose rate, No. cm Gy [ka.sup.-1] Hel-TL04251 KIL 1 80-78 2.109 [+ or -] 0.253 Hel-TL04252 KIL 2 141-111 1.914 [+ or -] 0.277 Hel-TL04253 KIL 3 231-158 1.962 [+ or -] 0.248 Hel-TL04254 KIL 4 268-258 1.884 [+ or -] 0.320 Lab. No. Dose, Age, Gy ka Hel-TL04251 86.0 [+ or -] 9.9 40.8 [+ or -] 6.9 Hel-TL04252 133.2 [+ or -] 14.1 69.6 [+ or -] 12.7 Hel-TL04253 141.7 [+ or -] 14.8 72.2 [+ or -] 12.1 Hel-TL04254 108.3 [+ or -] 15.4 57.5 [+ or -] 12.9 Table 3. Identified and dated plant macrofossils [sup.14]C sample Depth, No. cm KIL-1 258-252 258-252 KIL-2 273-268 273-268 273-268 KIL-3 310-295 KIL-3-2 310-295 KIL-4 355-350 KIL-4-2 355-350 KIL-5 375-365 KIL-6 545 [sup.14]C sample Determined species of No. plant macrofossils KIL-1 Schoenoplectus lacustris Nuphar lutea KIL-2 Schoenoplectus lacustris Najas marina Carex vesicaria KIL-3 Schoenoplectus lacustris, Betula pubescens KIL-3-2 Najas marina KIL-4 Betula alba, Populus tremula KIL-4-2 Najas marina KIL-5 Salix sp., Betula alba, Carex vesicaria KIL-6 Betula alba [sup.14]C sample Origin of plant No. macrofossils KIL-1 Terrestrial Aquatic KIL-2 Terrestrial Aquatic Terrestrial KIL-3 Terrestrial KIL-3-2 Aquatic KIL-4 Terrestrial KIL-4-2 Aquatic KIL-5 Terrestrial KIL-6 Terrestrial
|Printer friendly Cite/link Email Feedback|
|Author:||Lasberg, Katrin; Kalm, Volli; Kihno, Kersti|
|Publication:||Estonian Journal of Earth Sciences|
|Date:||Jun 1, 2014|
|Previous Article:||Postglacial occurrence and decline of Betula nana L. (dwarf birch) in northeastern Poland/Betula nana L. (vaevakase) jaaajajargne levik Kirde-Poolas.|
|Next Article:||Geological settings of the protected Selisoo mire (northeastern Estonia) threatened by oil shale mining/Polevkivikaevanduse ohustatud kaitsealuse...|