ARTICLE IN PRESS

Quaternary Science Reviews 23 (2004) 1391–1434

A review of postglacial emergence on Svalbard, Franz Josef Land and Novaya Zemlya, northern Eurasia S.L. Formana,*, D.J. Lubinskib, O.! Ingolfsson! c, J.J. Zeebergd, J.A. Snydere, M.J. Siegertf, G.G. Matishovg a Department of Earth and Environmental Sciences, University of Illinois, Chicago, IL 60607, USA b Institute of Arctic and Alpine Research, The University of Colorado, Boulder, CO 80309-0450, USA c Department of Geology and Geography, University of Iceland, Is-101 Reykjav!ık, Iceland d Netherlands Institute for Fisheries Research, Haringkade 1, P.O. Box 68 1970 AB IJmuiden, The Netherlands e Department of Geology, Bowling Green State University, Bowling Green, OH 43403, USA f Bristol Glaciology Centre, School of Geographical Sciences University of Bristol, University Road, Bristol BSS 1SS, UK g Murmansk Marine Biological Institute, 17 Vladimirskaya Street, Murmansk 183010, Russia

Abstract

The pattern of postglacial emergence in the Barents Sea is pivotal to constraining the timing of deglaciation and extent and thickness of the last ice sheet in northern Eurasia. This review unites records of Holocene relative sea level from Svalbard, Franz Josef Land, and Novaya Zemlya to better understand the geometries of past ice sheet loads. Emergence data from northern Eurasia confine the maximum area of glacier loading to the northwestern Barents Sea, where >100 m of emergence is measured on Kongs^ya. Deglacial unloading commenced on western and northern Spitsbergen c. 13–12 14C ka ago, and by c. 10.5 14Cka on eastern Svalbard and more distal sites on Franz Josef Land and Novaya Zemlya. The marine limit phase (c. 13–12 14C ka) on western and northern Spitsbergen is characterized by the construction of spits indicating a dominance of long-shore drift over storm- generated fetch, reflecting extensive sea-ice coverage of coastal areas. At sites in proximity to the ice sheet margin on western and northern Spitsbergen there is evidence for a transgressive–regressive cycle c. 6–4 14C ka, possibly reflecting back migration of displaced mantle material. A modern transgression is inferred from the marine erosion of 17th century cultural features and 14C ages of whalebone and terrestrial peat buried by modern storm gravels that place sea level at its present position by c. 2 to 1 ka ago. The greatest observed emergence on Franz Josef Land occurs on Bell Island, with a marine limit at 49 m aht, formed c. >10 14C ka. Available emergence data since 9 ka show rising strandlines toward the southwest at B0.3 m/km. The northern limit of emergence on Franz Josef Land is poorly constrained because relative sea-level data is sparse north of 80300N. In contrast to Svalbard and Franz Josef Land, the marine limit on northern Novaya Zemlya is only 10–15 m above high tide and formed between 6.5 and 5.0 14C ka when global sea level was stabilizing. All sites show little apparent emergence during the past 2 ka, with the youngest raised landforms at identical heights to storm beaches. This minimal glacio-isostatic signature on Novaya Zemlya and on Vaygach Island, where deglaciation commenced >10 ka ago, indicates ice sheet thicknesses of o1.5 km. The spatial variation in emergence for the Barents Sea indicates that western and northern Spitsbergen and Novaya Zemlya were near the reactive margin of the ice sheet and these areas sustained the briefest ice coverage (2–6 ka) and were probably not in isostatic equilibrium. In contrast, central and eastern Svalbard and southern Franz Josef Land were beneath a substantial ice load and probably sustained this load for c. 10 14C ka and achieved isostatic equilibrium. Isostasy residual from an ice sheet model portrays well the general pattern of uplift and load response at the centre of ice sheets, but deviates substantial at the ice sheet margin or areas covered by thin ice, like Novaya Zemlya. r 2004 Published by Elsevier Ltd.

1. Introduction distribution of past ice-sheet loads and deglacial history (e.g. Andrews, 1970). Observations on postglacial The pattern of postglacial emergence for many areas emergence are also important for developing a better in the Northern Hemisphere is pivotal in assessing the understanding of the glacio-isostatic adjustment process and the constraining properties of the underlying *Corresponding author. Fax: +1-312-413-2279. solid earth (Peltier, 1974, 1998; Cathles, 1975; Clark E-mail address: [email protected] (S.L. Forman). et al., 1978). Recent refinements in models of mantle

0277-3791/$ - see front matter r 2004 Published by Elsevier Ltd. doi:10.1016/j.quascirev.2003.12.007 ARTICLE IN PRESS 1392 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 viscoelastic structure and an improved understanding of However, in areas where post-glacial emergence was the extent and chronology of the Laurentide, Fennos- modest (o50 m), relatively brief (100 s to 1000 s of candian and Antarctic ice sheets provide a basis for years) arrests in sea level or transgressive–regressive estimating variations in ice sheet thickness during the events (o2 m) have been documented, reflecting the last deglaciation (Clark et al., 1994; Peltier, 1994, 1996; interplay between eustasy, isostasy, and steric and non- Lambeck, 1995). These earth rheological models accom- steric changes in sea level (Hafsten, 1983; Svendsen and modate site-specific relative sea level and global eustatic Mangerud, 1987; Forman, 1990; Fletcher et al., 1993; records (Fairbanks, 1989) providing new insight into the Forman et al., 1996; M^ller et al., 2002). Changes in the balance between ice sheet volume and changes in global course of relative sea-level on an emerging coastline are sea level in the past c. 20,000 yr (Tushingham and identified as constructional (broad raised terrace) or an Peltier, 1991; Peltier, 1994, 1996). erosional (escarpment) landform in the raised-beach In the last two decades of the 20th century large sequence, reflecting the complex interaction between sea uncertainties persisted on the geometry of late Pleisto- level, sediment supply, slope and wave energy (e.g. cene ice sheets and ice caps over the shelf seas bordering Elfrink and Baldock, 2002). the Arctic Ocean. Reconstructions of Late Weichselian The elevation of raised beach landforms was deter- ice sheet extent in the Barents Sea region range from a mined with either a barometric altimeter with an error of contiguous marine-based ice sheet over much of the 1–2 m or by transit or level with a precision of 10–30 cm. European arctic (e.g. Peltier, 1994, 1996; Lambeck, However, the relief on any one raised beach is usually 1– 1995), to smaller, coalescent ice caps based on arctic 2 m, which limits precision in assessing past sea level. archipelagos (e.g. Lambeck, 1995; Siegert and Dowdes- The datum for measuring the elevations across a raised well, 1995; Siegert et al., 1999; Svendsen et al., 1999). strand plain is the present mean high tide mark (m aht), This past disparity in ice sheet reconstructions reflected which is easily discernable on most coastlines as a swash the paucity of field observations to constrain the extent, limit. Coastal areas in the Barents Sea are microtidal thickness, and timing of late Quaternary glacial events with o2 m between high and low tide (Proshutinsky in northern Eurasia. A critical field observation to et al., 2001). The storm beach elevation varies across the determine the magnitude and distribution of past-glacier area attaining heights of 1–2 m within inner fjords and loads and the timing of deglaciation is the altitude and increasing to 4+m on exposed rocky headlands and age of raised-beach deposits. Quantitative studies on areas exposed to direct storm fetch (Forman, 1990; Svalbard defining the pattern of post-glacial emergence Zeeberg et al., 2001). Driftage is often conveyed and timing of deglaciation have been pursued since the further inland and beyond the storm beach limit up late 1950s (e.g. Feyling-Hansen and Olsson, 1959; Blake, valleys with the reverse flow of river discharge during a 1961a; Salvigsen, 1978, 1981, 1984; Forman et al., 1987; storm surge. Landvik et al., 1987; Forman, 1990; Salvigsen et al., 1990; Bondevik et al., 1995; Forman and Ingolfsson,! 2000; Bruckner. et al., 2002). Starting in the early 1990s 3. Radiocarbon dating the large expanse of the Russian Arctic became accessible to international scientific expeditions provid- Radiocarbon dating of driftwood, whalebone, walrus ing new Quaternary geologic data on former ice sheets. bone, seaweed and shell from raised-marine sediments This review unites observations on Holocene relative sea provides age constraint on marine inundation and level history for Svalbard (Norway) and Franz Josef deglaciation. Driftwood is the preferential subfossil Land and Novaya Zemlya (Russia) to assess patterns of collected from the raised-beach sequences because of postglacial emergence for areas that were beneath the its suitability for 14C dating and close association with Barents Sea/Eurasian ice sheet (Fig. 1). paleo-sea level. Often, the outer rings of driftwood logs were sampled to obtain 14C ages in close association with the sea level depositional event. If driftwood was 2. Near-shore conditions and the raised beach record not located, then whalebone and walrus-skull bone were retrieved for 14C dating. Bones were usually sectioned by The present altitude of raised beaches in the Eurasian saw and an internal, well-preserved dense part of the north reflects principally two competing processes; the bone was submitted for 14C dating. The collagen- postglacial rise in global sea level and isostatic up dominated gelatin extract from each bone was dated, warping of the lithosphere with disintegration of the last which in previous Arctic studies has yielded accurate 14C ice sheet that mostly occupied the Barents Sea. Global ages (e.g. Forman, 1990; Bondevik et al., 1995; Forman sea level has been relatively stable in the past 6000 yr et al., 1997) and have not given anomalous young ages, (Kidson, 1982; Fairbanks, 1989; Bauch et al., 2001) as bones from lower latitudes (Stafford et al., 1990). thus, raised beach elevation attained since the mid- Often the apatite fraction for whalebones or walrus- Holocene reflects predominantly isostatic compensation. skull bones was analyzed to evaluate the veracity of the ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1393

Fig. 1. Barents Sea region in northern Eurasia. Shown is most likely Late Weichselian ice sheet limits in northern Eurasia (from Alexandersson et al., 2002; Polyak et al., 2002; Svendsen et al., 1999). The limit of the last (Middle Weichselian; 60 ka) ice advance from the Barents Sea and Kara Sea onto the mainland is indicated by the Markhida Line (Mangerud et al., 1999). Also shown are uplift-isobases for 5000 14C yr BP in meters above present sea level. Thin dotted line is the 300 m bathymetric contour.

corresponding gelatin-based 14C age. If the apatite 14C Appendices A, B and C). This reservoir correction is age for the whalebone agrees at one sigma with the derived from pre-bomb shells from Nordic seas (Man- according 14C age on the gelatin extract, then the bone gerud and Gulliksen, 1975; Olsson, 1980). Epifaunal was a closed system for 14C. Starting in the late 1980s to shells collected in the late 19th century from Franz Josef early 1990s most 14C ages on shells are on a single valve Land and Novaya Zemlya yielded similar 14C values, by accelerator mass spectrometer (AMS) analysis, which though infaunal bivalves (Portandia arctica) yield ages circumvents earlier problems of dating shells of mixed of 760–600 years (Forman and Polyak, 1997). The age (Miller and Brigham-Grette, 1989). Prior to dating, radiocarbon timescale is used in this review because it is most shells received at least a 50% leach in HC1 to also the choice of the preponderance of previous studies. remove potential contaminants. To compensate for the Radiocarbon ages are converted to the calendar time- marine 14C reservoir effect, 440 yr was uniformly scale (Stuiver et al., 1998) only when used to test subtracted from all 14C ages on whalebone, walrus, modelled-ice-sheet-induced isostasy (Siegert and Dow- seaweed and shell assembled for this review (Table 1; deswell, 2002). ARTICLE IN PRESS 1394 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 ) 4 4 À 10 -value  k ( 6 2 Curve fit R 300 7 5 Uplift half-life (yr) 1.5 2000 4 7 Remnant uplift (C) (m) 3 0.3 2.9 7 1.1 0.5 0.6 1600 0.99 4.1 o Present uplift rate 2 90 25 limit B B 525 522 520 546 o o o o 38>40 321>65 31073 5 5 5 5 51148 o o o o o o o o 7 ka 9 ka (m aht) (mm/yr) 1 3 3 3 5 53 10 30 50+ 1.0 0.2 1300 0.56 5.5 5 3536 5 510 82764 654 3 97 8 20 5 12 26 17 55–60 25 65–75 65.5 90+ 1.1 0.9 2000 0.87 3.5 0000 57 1720312022 2620 2923 4517 37 4223 37 55 35 69 35 62 25 59 35 66 56 70+ 53 100+ 38 88.5 48 86.8 0.7 0.8 1.6 85.1 85–90 1.2 50 1.6 1.8 1.2 5.5 60+ 1.1 1.1 3.4 3.4 0.7 1.3 3.2 3.2 1800 1800 2300 1.7 0.99 4.0 0.99 0.97 2100 2100 0.99 2000 0.99 3.8 2100 3.8 3.0 0.99 0.99 1900 3.3 2300 3.3 0.97 0.98 3.2 3.3 3.6 3.0 10 20 45 o o o o o o o o 5ka ! olfsson (2000) ! e et al. (1982) . uckner et al. (2002) ! ew Jonsson (1983) Bondevik et al. (1995) Salvigsen (1978) Salvigsen (1981) Bondevik et al. (1995) Bondevik et al. (1995) Bondevik et al. (1995) Salvigsen and Mangerud (1991) Hoppe et al. (1969) Forman and Ing Salvigsen and Østerholm (1982) Salvigsen and Østerholm (1982) Br Blake (1961a) Lehman (1989) Forman (1990) Forman (1990) Forman (1990) Landvik et al. (1987) Ziaja and Salvigsen (1995) Salvigsen et al. (1991) Sandahl (1986) Forman (1990) Salvigsen et al. (1990) P Salvigsen (1984) Salvigsen and Slettemark (1995) Birkenmajer and Olsson (1970) ya ^ ya ^ ! eeland ya yane ^ ya ^ ya yra ^ ^ ^ ya ^ Norway , ya, Sj ya ^ ^ ya Island ^ ggerhalv rnoya ( ahuken ^ ^ Svartknausflya, Nordaustlandet Kongs Kapp Ziehen, Barents Humla, Edge Diskobukta, Edge Southern Edge Agardbukta Hopen Island Mean Table 1 Holocene emergence data and calculated uplift ratesLocality for Svalbard, Norway, and for Franz Josef Land, and Novaya Zemlya, Russia Reference Inferred emergence in meters since: Marine Gr Mosselbutka Woodfjord, Andr Lady Franklin Fjord, Nordaustlandet Stor Reinsdyrflya Phipps Mitrahalv Southern Prinz Karls Forland Br Ytterdalen, Bellsund Southern Sorkapp Land Wedel Jarlsberg Land, S. Bellsund Kapp Linne, Isfjorden Daudmanns Bohemanflya and Erdmannflya Blomesletta Kapp Ekholm, Billefjorden Svalbard Bj Hornsund ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1395 600 400 7 7 1.2 3000 1.5 2100 7 7 0.4 3.0 0.9 3.2 7 7 is time. Estimated remnant emergence extrapolated from curve t 0.8 1.1 is a time constant, and k is remnant emergence, C ) and rounded to nearest 100 years. k 999 11 13.5 12 0.5 0.7 0.5 1.6 4.0 1.8 2300 3500 0.85 0.94 3500 0.95 3.1 1.7 2.4 1010111011 12 13 0.6 12 1.7 10 11 1.6 4.4 0.8 0.9 0.9 3.7 2300 4.0 3500 2.5 0.99 0.78 3.4 3500 1.8 3300 0.97 2300 0.99 0.84 2.2 2.3 2.8 15 >21 24 0.9 3.4 2700 0.93 2.6 2022221820 2920 322418 28 4516 29 34 2618 3016 24 3217 49 2817 43 27 31 38 28 23 38–36 0.9 29 1.0 31 0.7 34 0.7 2.9 40 1.0 3.2 1.0 21 1.7 32 2.0 2.8 0.7 1.4 4.0 26 24 2200 4.2 2200 0.8 2.1 0.98 20 5.0 0.92 1500 2000 1900 0.9 7.6 0.7 0.85 2.6 0.94 3.2 0.99 2700 0.8 3.2 0.99 3.5 1.9 2000 4.8 2500 3.4 0.98 3.6 2.2 0.89 1300 2.6 2200 0.95 0.97 3.4 2.8 2600 1900 0.96 0.97 5.5 2000 3.2 0.98 2.7 3.6 3.5 is uplift, >20 38 1.1 3.2 2000 0.95 3.4 U =ln 2/ 1/2 t where kt e C ¼ C yr BP. U 14 Forman et al. (1999a,b) Zeeberg et al. (2001) Zeeberg et al. (2001) Zeeberg et al. (2001) Zeeberg et al. (2001) Zeeberg et al. (2001) Zeeberg et al. (2001) Forman et al. (1999a,b) Glazovskiy et al. (1992) Forman et al. (1996) Forman et al. (1996) Forman et al. (1996) Forman et al. (1996) Forman et al. (1996) Lubinski (1998) Forman et al. (1996) Forman et al. (1997) Forman et al. (1997) Forman et al. (1997) Forman et al. (1997) Forman et al. (1997) Forman et al. (1997) Forman et al. (1997) Russia , Russia , ld Bay ^ value for exponential curve fit function to calendar corrected emergence data. 2 Cummulative postglacial emergence sinceLate 5,000 Weichselian to HoloceneEstimated marine contemporary limit. emergence rateThe extrapolated function from is a a negative curve exponential fit in function the relating form radiocarbonEstimated flotsam half-life dates of to emergence elevation R based on curve fit function ( 1 2 3 4 5 6 Cape Bismarck Cape Zhelaniya Ivanov Bay Russkaya Gavan Cape Medvezhy Velkitsky Bay Nordenski Mean Cape Spory Navolok Novaya Zemlya Alexander Island Franz Josef Land Southeast George Island Bell Island Northbrook Island Etheridge Island Hooker/Scott Keltie Island Hooker Island, Cape Dandy Nansen and Koettlitz Islands Leigh Smith Island Brady Island Heiss/Fersman/Newcombe Islands Hall Island Wilzchek Island Koldewey Island Klagenfurt Island Mean fit function. ARTICLE IN PRESS 1396 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

4. Svalbard (Salvigsen, 1981; Forman, 1990; Forman et al., 1997; Landvik et al., 1998). Whereas, on northern and western Raised marine landforms were first recognized scien- Spitsbergen postglacial emergence is usually confined to tifically on Svalbard by pioneering Scandinavian geol- 65 m aht or lower (Forman, 1990; Forman et al., 1997), ogists Nordenski^ld (1866) and De Geer (1919). indicating comparatively modest loads near or beyond Strandlines were first dated by radiocarbon by Fey- the margin of the ice sheet. The elevational limit of ling-Hanssen and Olsson (1959) and by Blake (1961a) in littoral processes from the last deglacial hemicycle is central Spitsbergen in Billefjorden and on northern termed the Late Weichselian marine limit (LWML) and Nordaustlandet, in Lady Franklin Fjord, respectively. is commonly demarcated by a broad constructional Intensive study of the Quaternary geology of many terrace which represents en echelon accreted storm forelands on Svalbard during the past two decades beach gravels or erosional landforms, such as an provides an improved understanding of the pattern of escarpment eroded into surficial deposits or bedrock. postglacial emergence and isostasy (Table 1; Appendix There are 28 separate assessments of post-glacial A; Fig. 2). Well-preserved and extensive Late Weichse- emergence for Svalbard (Table 1; Appendix A, Fig. 2). lian and Holocene raised beaches from 60 to 130 m aht In this review we summarize post-glacial emergence by occur on eastern Svalbard and islands in the Barents Sea considering records from western Spitsbergen and from reflecting the area of maximum ice sheet loading eastern Svalbard.

Fig. 2. Majority of post-glacial emergence curves for Svalbard, Norway (modified from Forman, 1990). ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1397

4.1. Western spitsbergen 1986). The oldest terrace sequence c.>140 ka old found between 80 and 55 m aht is highly dissected with only The raised beach sequence on Br^ggerhalv^ya which 20–40 m long remnants of the original surface preserved. is typical for western Spitsbergen (Forman et al., 1987; These deposits lack distinctive shoreline morphologies, Landvik et al., 1987; Forman, 1990; Andersson et al., can be traced intermittently and contain a silt-rich B- 1999) has been divided into three distinct age groups horizon that exceed 80 cm thickness. Deposits of an (Fig. 3) on the basis of the degree of terrace dissection, intermediate age, c. 60–80 ka (Forman and Miller, 1984; preservation of individual shorelines and the extent of Forman, 1990), occur between 44 and 55 m aht and pedogenesis (Forman and Miller, 1984; Mann et al., exhibit B horizon of 70–50 cm thickness. Moderate

Fig. 3. Vertical aerial photograph (S70-4231, copyright Norsk Polarinstitutt, Oslo) of Br^ggerhalv^ya, western Spitsbergen. Shown are a tripartite raised-beach sequence the oldest extending up to 80+m aht and dated to >120 ka. The youngest sequence is demarcated by Late Weichselian marine limit at 45 m aht and is expressed as a truncated spit-cusp, shown by arrows. Three large raised barrier beaches occur at 45, 37, and 39 m aht. Below 29 m aht, numerous discrete strandlines occur down to the modern shore (from Forman et al., 1984). ARTICLE IN PRESS 1398 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 dissection of these deposits has produced 100–200 m southern Prinz Karls Forland (Forman, 1990; Anders- laterally continuous terrace remnants, with subdued son et al., 1999). strandlines recognizable. A distinct change in geo- Two whalebones collected above the LWML on morphic expression occurs at 45 m aht (Fig. 3); the Br^ggerhalv^ya yielded infinite 14C ages (>36 ka) on terraces at and below this level exhibit exceptionally the collagen fraction, supporting pedologic and geo- well-preserved beach morphologies with B-horizons that morphic interpretations that middle Weichselian or are o30 cm thick. This prominent geomorphic bound- older raised beaches occur on Br^ggerhalv^ya (Forman ary is dated on Br^ggerhalv^ya and other areas of and Miller, 1984). Whalebone retrieved from the western and northern Svalbard at c. 13–11 ka (Forman LWML on Mitrahalv^ya at 20 m aht was dated to et al., 1987; Landvik et al., 1987; Lehman, 1989; 12,9607190 yr BP (Beta 10,986). The marine limit at Forman, 1990). these two sites was established essentially synchronously The lowest and youngest raised beach sequence on because Kapp Mitra and Br^ggerhalv^ya was either Br^ggerhalv^ya from the last deglacial hemicycle dis- unglaciated or deglaciated early at similar times (c. plays striking changes in beach ridge morphology with >13 ka) (Lehman and Forman, 1992). A whale rib altitude that can be related to the rate and direction of retrieved from a swarm of bones on the 37-m prominent relative sea level change (Fig. 3). Three large beach beach ridge dated to 11,7607430 yr BP (GX-9909). ridges between 20 and 45 m altitude have broad crests Because this is one of the oldest ages on Svalbard (100–200 m wide) and relief up to 5 m. Below 20 m aht, associated with postglacial raised beach deposits the numerous narrow (5–10 m) and low (o2 m) strandlines other half of the bone was dated by a second laboratory occur down to the present shore where a large barrier for verification. This second age, 11,8007180 yr BP (I- beach ridge is actively forming. 13,793), is well within standard deviation of the original On morphologic consideration alone, the Br^ggerhal- age, giving an added measure of confidence to the v^ya sequence below 45 m aht suggests that relative sea dating. Radiocarbon ages of c. 12.5–11 ka are also level initially fell slowly and was interrupted by at least associated with LWML landforms and deposits near three short periods of still stand or possibly transgres- Bellsund (Landvik et al., 1987) and southern Prinz Karls sions that caused the construction of three barrier Forland (Forman, 1990; Andersson et al., 1999) and to beaches with crests at 29, 37, and 45 m altitude (Fig. 3). the north in Woodfjord (Bruckner. et al., 2002). Following construction of the ridge at 29 m, sea level fell Whalebones from discrete strandlines below 30 m to rapidly leaving only minor multiple strandlines down to the present shore on Br^ggerhalv^ya range in age the present shore where a coarse, clastic beach is between 10,275790 yr BP (DIC-3122), and presently forming in response to an ongoing transgres- 92307340 yr BP (GX-9908) with most ages overlapping sion (Forman et al., 1987). The occurrence of morpho- at two standard deviations (Fig. 4). Similar apparent logically similar raised beach sequences on Kapp rapid rates (2–3 m/100 yr) of emergence have been Guissez and Mitrahalv^ya (Forman, 1990) to the north, documented for other sites on western Spitsbergen, with massive beach ridges near the marine limit (albeit at including Daudmanns^yra, Southern Prinz Karls For- different altitudes due to regional variations in isostatic land (Forman, 1990), Bellsund (Landvik et al., 1987), depression) succeeded at lower altitudes by minor ridges continuing to the modern shore strengthens this reconstruction of relative sea level dynamics. The other striking feature of this raised beach sequence is the occurrence of a breach in the 45 m shoreline accentuated by curved terrace remnants, oblique to lower beaches (Fig. 3). This breach may represent the cusp of a spit built when the LWML was established, and subsequently eroded. Spits typically form in shallow coastal waters where there is abundant sediment supply and long-shore drift predominates, rather than storm generated fetch. An ice-covered sea would have dampened severely the dominant westerly fetch and favored longshore drift in near shore leads to build a spit on Br^ggerhalv^ya. Later, ice-free coastal conditions could have caused a switch to modern wave conditions and intensity that resulted in the truncation Fig. 4. Late Weichselian and Holocene relative sea level for of the spit. Spit remnants have been identified at the Br^ggerhalv^ya, Spitsbergen. Note rapid fall in relative sea level c. marine limit on other forelands of western Spitsbergen, 9.5 ka and inferred trangressive and regressive event c. 6 ka (from including Mitrahalv^ya, Sars^ya, Daudmanns^yra and Forman et al., 1987). ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1399 and Erdmannflya and Bohemanflya (Salvigsen et al., 1990). The rapid emergence probably reflects an elastic crustal response to ice unloading c. 10,000 yr BP. Abundant evidence exists for a sea level oscillation in the middle Holocene across broad areas of western and northern Svalbard. Near Br^ggerhalv^ya, a whalebone at 5 m aht behind the modern storm beach at T^nsneset on the north shore of Kongsfjord yielded an age of 59007210 yr BP (GX-9899), indicating that middle Holocene sea level was similar or slightly higher than the present level (Fig. 4). Other sites along western Spitsbergen (Landvik et al., 1987; Forman, 1990), northern Spitsbergen (Bruckner. et al., 2002)andon Phipps^ya (Forman and Ingolfsson,! 2000) constrain this high sea-level event between 6 and 4 ka ago. This high stand is associated with a prominent constructional beach between Isfjord and Bellsund, on western Spitsbergen (Landvik et al., 1987) and erosion and truncation of older raised beaches on Phipps^ya (For- Fig. 5. Holocene relative sea level for Kongs^ya, Svalbard, which man and Ingolfsson,! 2000). This dated sea level event is exhibits the greatest post-glacial emergence in the Barents Sea (from Salvigsen, 1981). often associated with the first pumice level, which is widely recognized across Svalbard (Blake, 1961a; Salvigsen, 1978, 1984), but may have occurred up to 2 ka earlier on Erdmannflya and Bohemanflya, on the Emergence of Hopen, south of Edge^ya, shows unusual northern shore of Isfjord (Salvigsen et al., 1990). near linear emergence since c. 9.4 14Cka(Fig. 2), which may reflect initial emergence under a thinning ice sheet, 4.2. Eastern Spitsbergen and Svalbard with a subsequent declining rate of emergence post deglaciation. Emergence records from southern Nor- On Eastern Spitsbergen (Bondevik et al., 1995) and daustlandet (Salvigsen, 1978) and Edge^ya and Bare- islands in the Barents Sea, like Stor^ya (Jonsson, 1983) nts^ya (Bondevik et al., 1995) show a fluctuation of and Hopen (Hoppe et al., 1969), there is single emergence rate at c. 6 ka, which may reflect the middle generation of raised beaches usually exceeding 50 m Holocene transgression documented at other localities aht, indicating full coverage and erosion by the Barents where total emergence is o70 m (Forman et al., 1987; Sea ice sheet (Landvik et al., 1998). The pattern of Landvik et al., 1987; Forman, 1990; Forman and postglacial emergence for Nordaustlandet is not well Ingolfsson,! 2000; Bruckner. et al., 2002)(Fig. 2). constrained. Only two emergence records exist for this island (Blake, 1961a; Salvigsen, 1978), although it is one 4.3. The pattern of post-glacial emergence on Svalbard potential source for the ice sheet that covered the Barents Sea during the late Weichselian. The highest Abundant chronologic control places retreat of the deglacial standlines on Svalbard are recognized on Kong northern and western margins of the Barents Sea ice Karls Land in the western Barents Sea (Salvigsen, 1981; sheet on to Svalbard by c. 13,000–12,000 14C yr ago Ingolfsson! et al., 1995). Although most raised beaches (Forman et al., 1987; Mangerud et al., 1992; Svendsen close to the marine limit often are obscured by et al., 1992; Elverh^i et al., 1995; Lubinski et al., 1996; solifluction on Kongs^ya, levels slightly above 100 m Knies and Stein, 1998; Landvik et al., 1998; Kleiber have been identified (Fig. 5). On the west side of et al., 2000; Bruckner. et al., 2002). The LWML phase Svensk^ya raised beaches are traced to higher levels, to between c. 13,000 and 10,500 14C yr BP on many approximately 120 m aht, indicating potentially greater forelands on western and northern Spitsbergen is glacier loading toward Spitsbergen. The Kongs^ya characterized by the construction of spits, with long- raised beach at 100 m aht is securely constrained by a shore drift predominating over storm-generated fetch. 14C age on Larix sp. log of 9850740 yr BP (GSC-3039), The inferred dominance of long shore drift and the indicating full deglaciation by at least c. 10 14Cka paucity of driftage associated with the LWML may (Salvigsen, 1981). Marine limits of approximately 90 m reflect extensive sea-ice coverage of coastal areas of aht in Billefjorden, Spitsbergen and 85–90 m aht on western Spitsbergen, obstructing the passage of whales Barents^ya and Edge^ya (Bondevik et al., 1995) also and driftwood laden sea ice and dampening the indicate appreciable loading, with deglaciation of the prevailing westerly waves. A more sea ice dominated latter dated to c. 10–10.4 14Cka(Landvik et al., 1998). Nordic Seas c. 15–11 ka is consistent with diatom ARTICLE IN PRESS 1400 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 paleoceanographic proxies (Ko@ et al., 1993). The The disjunct timing for this sealevel event may reflect the presence of whalebone, albeit rare, however indicate complexities of relative sea level with a collapsing that sea ice periodically dissipated in the Norwegian forebulge and the back migration of the viscous mantle Sea to allow the migration of whales to Svalbard. eastward with deglaciation (Fjeldskaar 1994). A modern This variability in sea surface conditions is characteristic transgression has been inferred from the marine erosion of the last glacial maximum when there were sub- of 17th century cultural features (Feyling-Hansen, 1955; millennial-scale oscillations in the dominance of Blake, 1961b; Forman et al., 1987). Radiocarbon ages of North Atlantic and Arctic water masses off of Svalbard whalebone and terrestrial peat buried by the modern (Hebbeln et al., 1994; Dokken and Hald, 1996). The storm beach on western Spitsbergen support this rate of emergence during c. 13,000 and 10,500 14Cyr interpretation and indicate that sea level rose to its was relatively slow (1.5–5 m/ka) reflecting the rate present position c. 2000–1000 14CyrBP(Forman, 1990; of isostasy just exceeding eustatic rise of sea Andersson, 2000). level of approximately 15 m/ka for this interval Emergence curves from western and northern Spits- (Fairbanks, 1989). bergen provide the oldest (c. 13,00014C yr BP) but Relative sea level fell rapidly (15–30 m/ka) for many discontinuous post-glacial record of relative sea level for sites on western and northern Spitsbergen between Svalbard (Fig. 2). This pattern of emergence corre- 10,500 and 9000 14C yr BP with raised beaches deposited sponds well to predictions for sites that were at or near parallel to the present shoreline, indicating that wave the margin of a large ice sheet (Transition zone I/II of direction was similar to that of the present. Emergence Clark et al., 1978). In contrast, shoreline displacement commenced for areas on eastern Spitsbergen (Salvigsen on eastern Svalbard and islands in the Barents Sea and Mangerud, 1991), Barents^ya and Edge^ya (Bon- commenced c. 10,000 14C yr BP and is continuing at devik et al., 1995) and Kong Karls Land (Salvigsen, present (Forman et al., 1997). These records are similar 1981) post 10,500–10,000 14C yr BP. The presence of to relative sea level predictions for areas that were extralimital, thermophilous mollusk Mytilus edulis in beneath a substantial (>1 km) ice sheet load (Clark western (Salvigsen et al., 1992) and northern Spitsbergen et al., 1978; Lambeck, 1995, 1996). The spatial variation (Bruckner. et al., 2002; Salvigsen, 2002) starting 9500 in emergence recognized for Svalbard indicates that 14C yr BP and on Edge^ya c. at 9000 14CyrBP(Hjort western and northern Spitsbergen was near the reactive et al., 1995) is coincident with the ubiquity of whalebone margin of the ice sheet. Marine geologic studies on the on lower terrace surfaces indicate that summer sea ice continental shelf and slope north of the Barents Sea coverage was considerable less and near shore waters place advance of the last ice sheet Sea ice sheet to its were warmer (>1C) than present. This marine warmth northern limit by c. 21–23 14C yr BP and retreat of is a result of increased advection of North Atlantic northern areas of Svalbard and Franz Josef Land by c. waters c. 10,000 14C yr BP off of Svalbard (Ko@ et al., 15 ka (Leirdal, 1997; Kleiber et al., 2000). Thus, ice 1993) and into the Barents Sea (Lubinski et al., 2001; marginal areas on northern Svalbard potentially sus- Ivanova et al., 2002), coupled with heightened summer tained relatively brief ice coverage (3000–8000 yr), under insolation 70–80N at c. 11,000–7000 14CyrBP(Berger variable ice sheet or ice stream flow and were probably and Loutre, 1991). not in isostatic equilibrium, with glacio-isostatic unload/ A mid-Holocene (6–4 14C ka) transgressive–regressive load half life of B 2000 years (Forman and Ingolfsson,! cycle is recognized at many localities on western and 2000). In contrast, central and eastern areas of the northern Spitsbergen (Forman et al., 1987; Landvik archipelago, which deglaciated by at least c. 10.5 14Cyr et al., 1987; Forman, 1990; Forman and Ingolfsson,! BP (Landvik et al., 1998) were beneath a substantial ice 2000; Bruckner. et al., 2002). The transgression did not load and probably sustained this load for at least exceed 7 m of elevation and is demarcated by a 10,000 yr and achieved isostatic equilibrium. Earth constructional terrace that truncates early Holocene rheology-based ice sheet models which are predicated regressional strandlines. Radiocarbon dating of a on isostatic equilibrium often model well the former variety of marine subfossils associated with this trans- centers of ice sheets, but deviate from field observations gressive feature indicates that the sea occupied this level for non-equilibrium areas at the ice margin (Forman between 6000 and 4000 14C yr BP. Even in areas on and Ingolfsson,! 2000). eastern Svalbard where total emergence is >70 m there The decline in elevation (19 m aht) of the marine limit is a noticeable fluctuation in emergence rate centered at and associated isobases (Forman, 1990; Forman et al., 6000 14C yr BP, which may also reflect this sea level 1997; Landvik et al., 1998) in southernmost Spitsbergen oscillation (Salvigsen, 1981; Salvigsen and Mangerud, and no emergence on Bj^rn^ya (Salvigsen and Slette- 1991; Bondevik et al., 1995). However, one emergence mark, 1995) indicates minimal glacier loading and/or record from Bohemanflya and Erdmannflya places a early deglaciation (before 10 ka); the former is supported transgressive–regressive event considerably earlier be- from marine geologic records from the adjacent Bear tween 8000 and 7000 14CyrBP(Salvigsen et al., 1990). Island Trough (Faleide et al., 1996). ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1401

The pattern of post-glacial emergence since 9000 and Mijenfjord indicating areas of substantial ice sheet 5000 yr ago is assessed for Svalbard, Franz Josef Land loading. The 5000 14C yr BP isobase, though registering and for the latter period for Novaya Zemlya (Fig. 6). at least 50% less emergence than the 9000 14Cyr BP The combination of emergence data from Franz Josef isobase, portrays a similar pattern to older isobases, and Land, Svalbard and Novaya Zemlya is justified because thus is an effective measure of past glacier loading. glacio-isostatic compensation reflects past glacial loads over 100s of kilometers, with a half-life response of approximately 2000 years (Table 1). These isobases are 5. Franz Josef Land hand contoured from 14C-dated relative sea level records for individual raised strandplain sequences (Fig. 2; Raised beaches were initially recognized on Franz Appendices A and B). The 9000 14C yr BP isobase Josef Land during early geologic exploration (Koettlitz, defines a broad zone of maximum emergence through 1898). Dibner (1965) and Grosswald (1973) were the the east and centre of the Svalbard archipelago, with first to undertake a systematic study of post-glacial islands in the Barents Sea and eastern Svalbard emergence on Franz Josef Land. They identified registering greatest emergence. There is a noticeable extensive raised-beach sequences on Hooker, Hayes, deflection westward of isobases into Isfjord and Van Alexandra and other islands in the Franz Josef Land

Fig. 6. Estimated emergence isobases for the Barents Sea area since 5000 and 9000 14C yr. Circles indicate placement and value of emergence data points, which are listed in Table 1. ARTICLE IN PRESS 1402 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 archipelago. Most notably, they collected five driftwood beaches dominate the present shore of central and samples from raised beaches for 14C dating, providing eastern Franz Josef Land. Storm-beach gravels and sea- the first age constraints (c. 6000 yr) on deglaciation and ice-pushed ridges often extend up to 2–3 m above the emergence of Franz Josef Land. More recent contribu- present high-tide level. The tidal range on Franz Josef tions (Glazovskiy et al., 1992; Naslund. et al., 1994; Land is approximately 0.5 m (Denisov et al., 1993). Forman et al., 1995, 1996, 1997; Lubinski, 1998) There are 15 separate assessments of post-glacial contribute in total fifteen records (Table 1; Appendix emergence for Franz Josef Land (Table 1; Fig. 7), and B; Fig. 7) of postglacial relative sea level and strati- in this review we present as points of discussion graphic assessments on deglaciation for central and representative site from across the archipelago, includ- southern Franz Josef Land and are a basis for ing Bell, Hooker and Halls Islands. summarizing the pattern of post-glacial emergence. The studied islands, in the central and the southern 5.1. Hooker Island part of the archipelago, are bounded by sounds and fjords with water depths of >250 m (Matishov et al., One of the broadest forelands in the archipelago is on 1995). Most of the archipelago (85%) is covered by Hooker Island, rising to approximately 100 m aht, in the glaciers and all islands studied have low elevation fore of the Jackson Ice Cap (Fig. 8). This foreland was (o100 m aht) forelands covered partially by raised- initially studied by Forman et al. (1996), and was the beach sediments. Most sounds and fjords in the focus of more detailed assessment by Lubinski (1998), archipelago are covered usually by sea ice for 9–10 which provides a detailed record of postglacial emer- months of the year (Denisov et al., 1993). Sea ice gence (Fig. 9). A SPOT satellite image shows the inland conditions in the inter-island channels during July and limit of littoral deposition on Hooker and Scott Kelty August are variable, ranging from open water condi- Islands as a distinct lighter-toned surface that fills river tions to full sea-ice coverage. Gravel and boulder drainages (Fig. 8). This marine-limit depositional

Fig. 7. Holocene postglacial emergence records for Franz Josef Land, Russia (modified from Forman et al., 1997). ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1403

Fig. 8. Spot Image of Hooker and Scott Keltie Islands showing valley infills at the marine limit (36 m aht) and a prominent escarpment, below the Marine Limit (26 m aht) and associated with an arrest in sea level fall (from Forman et al., 1996).

Fig. 9. Elevation-age relation for raised beaches on Cape Dandy, Hooker Island, Franz Josef Land. This relative sea level curve is constrained by 23 14C ages from the Cape Dandy region (solid boxes), an additional 21 14C ages from raised beaches within 20 km of Cape Dandy support the relation (open symbols). Error bars are one standard deviation (from Lubinski, 1998). ARTICLE IN PRESS 1404 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 feature is composed of fluvially dissected, sandy to for emergence. A striking geomorphic feature is a 2–5 m gravelly, shallow-water marine sediments. Paired valves high escarpment at approximately 26 m aht eroded into of Mya truncata, with periostracum and siphon pre- beach gravels and bedrock. A 14C age on driftwood served and collected from the lower part of the marine deposited against the escarpment places the erosional deposit yielded 14C ages of 10,2907115 yr BP (GX- event before 6000 yr BP. A prominent raised accre- 17266), 9995785 yr BP (AA-8566) and 9645780 yr BP tionary spit occurs at 1672 m aht; a 14C age on a whale (AA-8567). The marine limit at 3672 m aht on jaw bone from the cusp of the spit places construction at interfluves is recognized as the boundary between c. 4300 yr BP. On Bell Island, the lowest identified washed, rounded gravels and an unsorted glacial drift. raised-beach surface is at 1 m aht, situated about 100 m A whalebone from 33 m aht on a regressional strand behind the modern storm beach. Driftwood imbedded immediately below the marine limit yielded the 14C age into this raised beach surface yielded the 14C age of of 94157125 yr BP (GX-17197G), providing a mini- 1050795 yr BP (GX-19476G), indicating that emer- mum age for the initial fall in postglacial sea level. gence is nearly complete. On Hooker Island a broad constructional marine terrace commonly occurs approximately 6 m below the 5.3. Hall Island marine limit. Driftwood embedded near the crest of this terrace at 29 m aht gave 14C ages 87157100 yr BP (GX- Field studies concentrated on the southeastern gla- 17198) and 72457100 yr BP (GX-17556) and indicate cier-free forelands on Hall Island. The limit of marine that relative sea level was stable during this interval. A influence was identified to 3272 m aht as a washing more detailed study of emergence that generated 23 limit eroded into drift-covered bedrock. Associated with additional radiocarbon ages constrains this arrest this washing limit is a discontinuous constructional between c. 9.0 and 7.8 14Cka(Lubinski, 1998). Initial beach with superimposed ice-pushed ridges (cf. Martini, observations of a broadening in the regressional 1981) that crests at 32 m aht. These well-preserved sequence at 1772 and 872 m aht, corresponding to c. marine limit features are within a few 100s-of-m of the 5500 14C yr BP and 3500–3000 14C yr BP, that were present margin of outlet glaciers of the Hall Island ice interpreted as arrests in emergence (Forman et al., cap. A 14C age of 86557145 yr BP (GX-19495) on 1996). Subsequent detailed dating of a raised beach driftwood from a regressional strandline, approximately sequence at Cape Dandy (Fig. 9) does not indicate any 1 m below the marine limit, provides a minimum change in emergence rates corresponding to these constraining age on deglacial emergence. Driftwood elevations or ages (Lubinski, 1998). located inside Severe Bay at 23 m aht gave the 14C age of The lowest raised beaches at 1–2 m aht on Hooker 83107145 yr BP (GX-19512), at least 1000 years Island, at the head of Calm Bay (Fig. 8) are protected younger than the inferred age of the equivalent raised from storm waves that form 2–3 m high storm beaches beach outside the bay. This log was found at the base of on the outer coast of the island. Partially buried logs a scree slope and may have been retransported down- from raised surfaces at 1 and 2 m aht yield 14C ages slope with postglacial regression. 775765 yr BP (GX-17200) and 1100780 yr BP (GX- A sequence of marine sand beneath raised-beach 17199) indicating little remaining emergence. Surpris- gravels along the inner part of Severe Bay herald even ingly, a log buried at 0.5 m aht gave the 14C ages earlier deglaciation (Forman et al., 1997). Exposed in >38,000 yr BP (GX-17201), the only evidence for open stream and coastal sections is a sequence of stratified water conditions before the Late Weichselian. sand and silty-sand, containing isolated drop stones. Centimeter-scale beds fine upward from a medium to 5.2. Bell Island coarse sand to a sandy-silt. Throughout the sequence there occur paired mollusks of Macoma calcarea and The highest marine terrace on the archipelago is Mya truncata, and other marine fauna. The presence of identified at 4972 m aht inset against a steep bedrock abundant paired mollusks with periostracum and hinge slope on southeastern Bell Island (Forman et al., 1996). ligament, and common burrowing structures indicates Radiocarbon ages of 92207120 yr BP (GX-17209G) an in situ fauna. Most notable is an increase in bed dips and 97057105 yr BP (GX-17208) on whalebone and from 5 to 10 at the section base to 25 to 30 up- driftwood imbedded in regressional gravels at 4772 and section, concomitant with a general coarsening in the 4572 m aht, respectively provide minimum limiting ages sand fraction. The plunge of the beds (155–120) on emergence. Below the marine limit there are a series indicates a sediment source from the northwest, toward of steeply inclined marine terraces covered by eolian the present outlet glacier margin. The sequence was sand. truncated with regression and emplacement of beach On southwestern Bell Island a gently sloping foreland, gravels on top of the section. Radiocarbon ages on covered by raised beaches to approximately 30 m aht paired Mya truncata shells from this sequence place provides an optimal setting for resolving a time series deposition of these near-shore sands between c. 8300 ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1405 and 9700 14C yr BP. This sedimentary sequence repre- the marine limit may indicate a more permanent coastal sents deltaic sedimentation immediately in front of a sea-ice coverage that would dampen waves and restrict glacier margin. The lowest, shallowly inclined beds (dips the flux of flotsam during initial emergence (cf. of 5–10) mark bottom-set deposition. The overlying Haggblom,. 1982). more steeply inclined beds may reflect progradation of There is evidence that emergence is nearly complete the delta front with fall or stabilization of relative sea on Franz Josef Land. Driftwood 1–2 above the storm level, or slight advance of a nearby (within 0.5 km) beach limit yielded 14C ages between 775 and 1500 yr outlet glacier. BP, indicating emergence rates for the past millennium of o1–2 mm/year (Table 1). Similar low rates of 5.4. The pattern of postglacial emergence for Franz Josef emergence in the past millennium in Fennoscandinavia Land are characteristic of areas that sustained modest Late Weichselian ice sheet loads (o1500 m) within a few 100s Radiocarbon ages on in situ mollusks and one piece of km of the inferred ice sheet margin (Emery and of driftwood place deglacial invasion of the sea along Aubrey, 1991; Fjeldskaar, 1994). British Channel at or before 10,400 14CyrBP(Forman et al., 1996). A number of 14C ages between 9200 and 9700 14C yr BP on driftwood and whalebone o10 m 6. Northern Novaya Zemlya below the marine limit clearly show that forelands adjacent to British Channel were deglaciated by the The first scientific expeditions to Novaya Zemlya early Holocene. Raised glacial-marine and deltaic identified raised beaches up to 100+ m, which were sediments dated between 9.7 and 8.3 14C ka within assumed to reflect glacio-isostatic unloading from a Late 1 km of present glacier margins indicate that outlet Weichselian glaciation (Gr^nlie, 1924; Zagorskaya, glaciers were at or behind present limits during the early 1959; Kovaleva, 1974; Grosswald, 1988). The occur- Holocene (Lubinski et al., 1999). Limited marine rence of raised beaches >100 m in elevation on Novaya geologic studies of interisland channels on Franz Josef Zemlya, similar to areas at the former centre of ice Land place deglaciation by c.10–9.6 14CyrBP(Polyak sheets in central Canada and Fennoscandinavia, is an and Solheim, 1994; Lubinski, 1998). It remains un- important criterion for reconstructing a 3-km-thick ice certain whether unstudied areas to the northeast, like sheet centered over Novaya Zemlya (Lambeck, 1995; Graham Bell Island, share a similar glacier history. The Peltier, 1996). However, observations in the 1990s regional pattern of postglacial emergence indicates that (Forman et al., 1995, 1999a, b; Zeeberg et al., 2001; past glacier loads were greater over the adjacent Barents Zeeberg, 2002) of the raised marine record on northern Sea than Franz Josef Land (Figs. 6 and 10). The Novaya Zemlya places the postglacial marine limit a maximum-recorded glacio-isostatic compensation for magnitude lower at c. 15–10 m aht. Rheological model- Franz Josef Land is toward the southwest, on Bell ing with this lower glacio-isostatic response yields an ice Island, with a marine limit at 4972 m aht, formed c. sheet centered on the Barents Sea and terminating into 10,000 14C yr BP. The lowest recognized emergence is on the Kara Sea with an inferred thickness of o1500 m the easternmost island studied, Klagenfurt, with a over Novaya Zemlya (Lambeck, 1995). Presented in this marine limit of 2072 m aht dated at c. 6000 14Cyr section are the studied localities from the northern and BP. Emergence isolines further east and north are not southern Barents and Kara Seas coast and for Vaygach well constrained because of the paucity of relative sea- Island that principally constrain post-glacial emergence level data, especially north of 80300N. The available (Figs. 1 and 11). emergence data since 9 and 5 ka show these raised surfaces respectively ascending toward the southwest 6.1. Kara Sea coast: Cape Bismark and Cape Spory into the Barents Sea at approximately 0.3 and 0.1 m/km Navolok (Forman et al., 1996). There is a clear absence of cobble or boulder beaches The marine limit is demarked in a bay south of Cape at the marine limit, though clastic beaches are common Bismark by a well-developed raised beach berm that lower in the regressional sequence and at the present varies in elevation between 12.5 and 13.5 m aht. The shoreline. The highest level of marine incursion is western end of the berm consists of rounded beach commonly demarcated by a discrete washing limiting pebbles and terminates against frost-shattered, lichen- eroded into glacial drift and in many valleys, particu- covered bedrock. Driftwood collected immediately larly on Hooker Island, is coincident with sandy marine behind the berm and 14C dated to 5365760 yr BP infill. There is also a noticeable paucity of driftwood and (GX-25466; Zeeberg et al., 2001) provides a close whalebone associated with the marine limit surface limiting age on initial emergence (Fig. 11). A whale (Forman et al., 1996; Lubinski, 1998). The lack of vertebrae and driftwood collected behind the berm boulder-dominated beaches and a paucity of driftage at yielded anomalous young ages of c. 3710 14CyrBP ARTICLE IN PRESS 1406 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Fig. 10. Estimated emergence isobases for Franz Josef Land, Russia since 5000 14C yr BP and 9000 14C yr BP. Circles indicate location and value of data points. Data for Franz Josef Land are shown in Fig. 7 and listed in Table 1 (from Forman et al., 1997).

(GX-25467) and 3485 14C yr BP (GX-24850) respec- nearby Cape Bismark indicate that the elevation of tively, and probably were carried over the berm crest 1872 m aht estimated for this log is probably too high during later storm surges. The modern storm beach limit and it has been re-assigned an elevation of B12 m at Cape Bismark is 6.4 m aht, reflecting exposure of the (Zeeberg et al., 2001). bay to a predominately southeastern fetch. The marine limit at Cape Spory Navolok, a headland 6.2. Kara Sea coast: Cape Zhelaniya projecting B4 km into the Kara Sea 15 km south of Cape Bismark, is a distinct wave-abraded escarpment at The marine limit in the Cape Zhelaniya area lies 7–11 m aht (Zeeberg, 1997; Forman et al., 1999a, b). A between a 10.5 m-high berm crest southwest of Cape diamicton above this escarpment at 1271 m aht is Mavriki and unwashed diamicton at 13 m aht. The unwashed. Previously, a driftwood log (48607140 storm beach limit at Cape Zhelaniya is B1.5 m, 14C yr BP (GX-18532) was retrieved at Cape Spory indicating low wave run-up. Cape Zhelaniya is a Navolok by Grosswald (Forman et al., 1995). The B500–200 m-wide promontory protruding about emergence curve and marine limit at B13 m aht for 1.5 km into the Kara Sea. The pattern of postglacial ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1407

Fig. 11. Post-glacial emergence curves for northern Novaya Zemlya (from Zeeberg et al., 2001) and Nordenskj^ld Bay (Forman et al., 1997).

emergence for the Cape Zhelaniya area is constrained by Zhelaniya. Similar platforms were observed at the samples from Cape Mavriki, Cape Serebryannikov, and Orange Islands, about 25 km NW of Cape Zhelaniya. a sequence in the B600 m-wide bay east of Cape Mavriki. A heavy driftwood root section provides the 6.3. Barents Sea coast: Ivanov Bay oldest (4380760 14C yr BP; GX-25459) and highest (7.0 m aht) sample (Appendix C). This sample was The marine limit at Ivanov Bay is demarked by a collected from rounded cobbles on a bedrock notch, prominent raised berm that infills a 2 km-wide valley up indicating a washing limit at 9.5 m aht at the base of a to 13.5 m aht. Skeletal remains of a beached whale escarpment with active solifluction. scattered over this berm at 11.5 and 12 m aht yielded There is a possible washing level above the Holocene ages of 64457105 14C yr BP (GX-24843) and 66407105 marine limit (B13 m) between 20 and 30 m aht. These 14C yr BP (GX-24844), providing the oldest age con- older marine shoreline features include erosional straint for the marine limit on north Novaya Zemlya notches in bedrock at Cape Mavriki and prominent (Table 1). The highest raised beach at the foot of the horizontal, beach-like platforms at B24 m aht at Cape berm at 8.8 m aht is dated to 37607 45 14C yr BP (GX- ARTICLE IN PRESS 1408 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

25464). Modern wood was encountered up to 4.3 m aht 6.6. Vaygach Island in Ivanov Bay and on its western cape (Cape Varnek). Driftage at both locations included German sea mines The marine limit was assessed in the summer of 2000 from the 1940s at 2 m aht, indicating low storm surge on Vaygach Island around Cape Bolvansky and Cape activity in the past B60 years. Diakanova, respectively the northern and southernmost capes of this 100 km-long island. The marine limit was found to coincide with the modern storm beach at B2m 6.4. Barents Sea coast: Cape Medvezhy aht. Radiocarbon ages on weathered, probably in situ driftwood collected among modern, sawn logs on Cape A detailed record of emergence was established on a Bolvansky, indicate little (o2 m) relative sea level 4 km long stretch immediately southwest of Cape change in the past B6 centuries (Zeeberg et al., 2001). Medvezhy. This area is exposed to Barents Sea storm surges resulting in storm run-up to 6 m aht in stream 6.7. Post-glacial emergence on Novaya Zemlya valleys. Driftwood associated with the modern 4 m-high storm ridge encroaches onto the slightly lower raised The marine limit formed on northern Novaya Zemlya beach. Subfossil driftwood partly buried in this surface between 6500 and 5000 14C yr BP when global sea level at 3.8 m aht yielded an age of 295750 14C yr BP (GX- was stabilizing (Kidson, 1982; Fairbanks, 1989; Bard 24858; Appendix C), indicating little to no effective et al., 1996). All sites show little apparent emergence emergence in the past B400 years. The raised beach during the past 2000 years, with the lowest raised sequence terminates against a B5 m high escarpment, landforms at identical heights to storm beaches (Fig. and the highest discernable raised beach was found at 11). The emergence curves for north Novaya Zemlya 10.5 m aht. A driftwood log at 10.3 m aht behind this (Fig. 11; Table 1) indicate an average uplift-rate of ridge yielded an age of 4070755 14C yr BP (GX-24864). B0.8 mm/yr at present and B2.5 mm/yr between 5000 Two kilometers to the south of this location the and 4000 14C yr BP. However, a 35 yr-long tide gauge regressional littoral fill against the escarpment record from Russkaya Gavan polar station yields extends to 12 m aht, demarking the marine limit for modern uplift rates of 2 mm/year for north Novaya this area. Zemlya (Emery and Aubrey, 1991; p. 144). The lower uplift rates based from the raised beach record probably reflects the influence of wave-run up, which often 6.5. Barents Sea coast: Russkaya Gavan redeposits driftage to a higher elevation, near the storm beach limit, yielding young ages for the lowest raised Russkaya Gavan (Russian Harbor) is a 10 km-long by beaches and resulting in artificially depressed uplift 5 km-wide fjord that runs N-S (Fig. 11). The emergence rates. Uplift rates during the past B4000 yr, were sequence studied is on a B400 m-long beach in a 2 km- relatively low (o2.5 mm/yr) and may partially reflect wide bay separated from the main fjord by a promon- low elevation of raised beaches (10–15 m aht) effected by tory. The storm beach is o2 m high. A series of raised variability in wave run-up. Thus, apparent uplift rates of beaches descends from a well-defined raised berm at 0.8 mm/yr and uplift half-lives of 3000 yr for the past 11.5–12.5 m aht, which is cut by a meltwater stream B4000 yr may be underestimates and the actual half- draining a valley parallel to the Shokalski Glacier. The lives are probably shorter, between 2000 and 3000 years marine limit is demarked by a clear contact between (Table 1). rounded pebbles and bedrock covered by a thin Ice retreat from coastal areas of northwest Novaya (o0.5 m) diamicton, containing angular, poorly sorted Zemlya is constrained by the c. 8000 and 8700 14CyrBP clasts. Subfossil driftwood is found between 2 and 4 m shell ages from Ruskaya Gavan (Zeeberg et al., 2001) aht, but is rarer at higher elevations. The highest and a basal age of c. 9240 14C yr BP on a marine core retrieved driftage is a 2 m-long log at 6.5 m aht, which from Nordenski^ld Bay (Forman et al., 1999a, b). Initial yielded an age of 4145750 14C yr BP (GX-24857; retreat of outlet glaciers on Novaya Zemlya is poten- Zeeberg et al., 2001). The general scarcity of driftwood tially coincident with cessation of glacial marine and low-elevation storm beach probably reflect the bay’s deposition in northern and eastern Barents Sea at c. sheltered topography and position to Barents Sea storm 10,000 14Cyr BP (Polyak and Solheim, 1994; Polyak run-up. et al., 1995, 1997, 2000; Lubinski et al., 1996; Hald and A pronounced bedrock notch at B23 m on the Aspeli, 1997) and the onset of postglacial emergence on promontory north of polar station Russkaya Gavan Franz Josef Land and eastern Svalbard c. 10,000 14Cyr possibly indicates a pre-Holocene washing limit. This BP (e.g. Bondevik et al., 1995; Forman et al., 1995, 1996, level appears to be similar to the pre-Holocene levels 1997; Landvik et al., 1998). Older minimum limiting found at Cape Mavriiki, Cape Zhelaniya, and the deglacial ages of c. 13,000 14C yr BP have been obtained Orange Islands. on marine cores from the deep (water depths >450) ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1409 troughs in the northern shelf of the Barents Sea 7. The marine limit and deglaciation in the Barents Sea (Lubinski et al., 1996; Polyak et al., 1997; Hald et al., 1999; Kleiber et al., 2000). Nearby sediment Available chronologic control from land areas and the records from the continental slope in the Arctic Ocean continental shelf places retreat of the northern and suggest that initial decay of the Barents Sea ice western margins of the Barents Sea ice sheet by c. 13,000 sheet along its northern margin began c. 15 ka (e.g., 14Cyr BP (Forman et al., 1987; Svendsen et al., 1992; Knies and Stein, 1998; Knies et al., 2001; Kleiber et al., Polyak and Solheim, 1994; Elverh^i et al., 1995; 2000). Lubinski et al., 1996; Bruckner. et al., 2002). Stable Early Holocene uplift of Novaya Zemlya, prior to isotopic and IRD records from the continental slope in formation of the marine limit (B6000 14C yr BP), is the Arctic Ocean suggest that initial decay of the Barents extrapolated from the relative sea level record. Calcu- Sea ice sheet along its northern margin began c. 15,000 lated uplift rates of 5–6 mm/yr between 9000 and 6000 14C yr BP ka but that major grounding line retreat off 14C yr BP indicate that about 15–20 m of uplift occurred the shelf may not have begun until c. 13,500 ka (e.g., during this period, compared to about 40 m of global Knies et al., 1999, 2000; Kleiber et al., 2000). Geo- sea-level rise (Kidson, 1982; Fairbanks, 1989; Bard et al., morphic and stratigraphic evidence place deglacial 1996). Thus, it is inferred that sea level rise outpaced unloading of central Franz Josef Land prior to 10.0– uplift, implying a transgression until cessation of global 10.4 14Cka (Forman et al., 1996, 1997); a similar sea level rise c. 6000 14C yr BP. Isostatic rebound conclusion has been reached for eastern Svalbard dominated postglacial eustatic sea-level rise after c. 6000 (Landvik et al., 1998). The apparent age difference 14C yr BP, resulting in formation of the marine limit and between deglaciation of the deep troughs in the northern regression to the present shore. Novaya Zemlya’s Barents Sea at c. 13 ka and the adjacent Franz Josef uniformly low (15–10 m aht) marine limit is similar to Land at c. 10.4 ka may reflect relict glacier cover given the marine limits found in southwest Scandinavia that glacial marine sedimentation occurs in the troughs (Svendsen and Mangerud, 1987) and on northwest and until c. 10 ka (e.g., Lubinski et al., 1996). Nevertheless, a south Svalbard at the thinning edge of the Barents Sea hiatus in datable material delivered to the archipelago ice sheet (Forman, 1990; Ziaja and Salvigsen, 1995; cannot be ruled out. Forman and Ingolfsson,! 2000). Based on these studies There is a distinct absence of boulder-dominated and assuming a comparable rheological response to beaches at the marine limit on Franz Josef Land, though unloading, Novaya Zemlya’s low Holocene marine limit boulder beaches are common lower in the regressional and current uplift rates of B1–2 mm/yr reflect a Late sequence and at the present shoreline. The highest level Weichselian ice load o1000 m (Lambeck, 1995, 1996; of marine incursion is demarcated commonly by a Peltier, 1996). discrete washing limit eroded into glacial drift, or in Isostatic uplift on north Novaya Zemlya since proximity to a sediment source, constructional beach 5000 14CyrBP is 1071 m on the east coast (capes ridges in valley mouths. There is a noticeable lack of Bismark and Spory Navolok) and the west coast driftage on the marine-limit surface. Only two pieces of (Ivanov Bay and Cape Medvezhy). Lower uplift values driftwood, one from Hall Island and the other from of 871 m aht since 5000 yr at Cape Zhelaniya and Koldewey Island, were retrieved after surveying numer- Russkaya Gavan probably reflect low wave run-up, ous marine-limit landforms on central and eastern Franz resulting in driftwood deposition at lower elevations. Josef Land. A similar paucity in driftage on marine-limit Isostatic uplift since 5000 14CyrBPis1171 m in the surfaces was observed on western Franz Josef Land Nordenski^ld Bay 300 km south of our northern (Naslund. et al., 1994; Forman et al., 1996). The lack of study area, suggesting that the isobase pattern runs boulder-dominated beaches, occurrence of sea-ice parallel to the Novaya Zemlya coastline (Fig. 6). pushed ridges, and scarcity of driftage on marine limit Furthermore, the similarity of uplift on Cape Medvezhy surfaces may indicate a more permanent sea-ice cover, at and Cape Bismark, areas with comparable storm least in the near-shore zone, that would dampen waves run-up on opposite sites of the island, suggests little and restrict the flux of flotsam during initial emergence differential uplift across the B80 km width of Novaya (Haggblom,. 1982; Stewart and England, 1983). Zemlya (no east–west tilt) since 5000 yr BP. There The oldest 14C ages on driftage and shells of c. 10.4 ka are no Late Weichselian or Holocene raised marine from raised marine deposits on Franz Josef Land sediments along the mainland coastlines of the (Forman et al., 1996) and eastern Svalbard provide a Kara Sea and southwest Yamal Peninsula (Mangerud, minimum age on deglaciation, particularly if perennial et al., 1999; Forman et al., 1999a, b). This, and sea ice dominated with ice sheet retreat. A permanent the absence of Holocene raised beaches on northern- sea-ice cover would restrict the flux of flotsam (H- most Vaygach Island, implies that the line of aggblom,. 1982; Stewart and England, 1983), the in- zero-emergence runs immediately south and east of migration of whales (Moore and Reeves, 1993), and Novaya Zemlya. colonization by mollusks (Peacock, 1989). Diatom ARTICLE IN PRESS 1410 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 records for the Norwegian and Greenland seas indicate evidence that outlet glaciers were at or behind present a perennial sea-ice pack between c. 13 and 10.5 ka, with margins by the early Holocene (Forman et al., 1996, present sea-surface conditions prevailing by 10 ka (Ko@ 1997; Lubinski et al., 1999). Blake (1989) reports AMS et al., 1993). However, planktonic foraminferal records 14C ages of c. 9.7–9.2 ka on shell fragments from an west of Svalbard indicate periodic open water conditions interlobate moraine from a northern outlet of the in the late glacial (Hebbeln et al., 1994; Dokken and Nordaustlandet ice cap. These ages indicate that this Hald, 1996). The occurrence of whalebones, though outlet retreated at least 6 km from its current position rare, dated between 13 and 11 14C ka indicates episodic during the early Holocene to allow marine incursion and open-water conditions extending to nearshore areas on deposition of shells. On Stor^ya, a small island, 15 km west Spitsbergen (Forman et al., 1987; Forman, 1990). east of Nordaustlandet, the inferred presence of c. 9– However, there is a distinct absence of whalebone and 5 ka old raised beach deposits beneath the present ice driftwood c. >10 ka. on northern Spitsbergen, even cap marks a significant reduction or possible absence of though strandplains formed >11 ka, indicating the the ice cap during the early Holocene (Jonsson, 1983). A absence of open water conditions conducive for the similar geomorphic relation was recognized on Alexan- transport of driftage upon deglaciation (Salvigsen and dra Island, Franz Josef Land, where raised beaches Østerhlom, 1982; Lehman, 1989; Bruckner. et al., 2002). dated between c. 6800 and 5000 14C yr BP are Perennial sea-ice cover may have dominated northern juxtaposed at the present ice-cap margin, evidence for Svalbard and Franz Josef Land during the late glacial less glacier cover during the early Holocene (Glazovskiy until northward propagation of regional oceanographic et al., 1992). warming after 10.5 ka (Ko@ et al., 1993; Polyak et al., 1995; Lubinski et al., 2001; Ivanova et al., 2002). The first-order dimensions of the Late Weichselian 8. Postglacial emergence in the Barents Sea Barents Sea ice sheet are indicated by the maximum uplift pattern in the northwestern Barents Sea, along There is abundant evidence for pre-Late Weichselian with the position of moraines on the shelf edge north of raised beach features on western and northern Spitsber- Spitsbergen (Elverh^i et al., 1995; Leirdal, 1997, in: gen and on Novaya Zemlya. These basic field observa- Forman and Ingolfsson,! 2000) and around Bear Island tions indicate that the last glaciation was not the most (Salvigsen and Slettemark, 1995). These constraints extensive, nor resulted in the greatest ice sheet loads in imply an ice dome with a radius of B500 km. The the late Quaternary. The most extensive older raised eastern limit probably terminated in the Kara Sea beach sequence occurs on western and northern (Polyak et al., 2002) with ice flow likely following Spitsbergen, where well-preserved remnants occur up bathymetry. Major ice streams descended into the Franz to 40 m and above the Late Weichselian marine limit Victoria, St. Anna and Voronin Troughs while ice also (Forman et al., 1984; Mann et al., 1987; Forman, 1990). spread into the southern Barents Sea (Lubinski et al., Many of these surfaces, particularly on western and 1996; Polyak et al., 1997, 2000; Siegert et al., 1999; northern Spitsbergen (Forman et al., 1984; Forman, Kleiber et al., 2000). There is compelling evidence for a 1990; Andersson et al., 1999) show no evidence for subsidiary ice stream that flowed eastward across the glacier over riding while other sites show coverage by a northern Kara Sea and terminated on the Taymyr thin discontinous diamiction associated with the last Peninsula (Alexandersson et al., 2002; Polyak et al., glaciation (Mangerud et al., 1992; Forman et al., 1997). 2002). The ice dome in the Barents Sea and a potentially Direct dating of subfossils from these older deposits and smaller form over Novaya Zemlya drained to the correlation to nearby stratigraphic sections place these southwest with an ice stream into the Bear Island high relative sea level events c. 60–80 ka and >140 ka Trough. Eastward ice flow from the Barents Sea dome ago (Forman et al., 1987; Miller et al., 1989; Forman, toward Novaya Zemlya would have to overcome 1999). Washing levels are also identified at a number of accelerated flow into the St. Anna Trough and then sites above the Holocene marine limit at B24 m aht on overtop Novaya Zemlya’s steep and high (1000 m) north Novaya Zemlya (Zeeberg et al., 2001). These topography. Mountains and plateaus of Novaya Zem- northern levels are probably related to raised beach lya, therefore, may have sustained a satellitic ice dome deposits between 20 and at least 36 m aht in Nor- during the last glacial maximum, consistent with the denskj^ld Bay about 175 km to the southwest, which coast-parallel isobases at 5 ka (Zeeberg et al., 2001). yielded shell ages of >30 ka and are interpreted to Glacier cover of islands in the Barents Sea was reflect ice loading by an Early or Middle Weichselian ice probably reduced compared to present glacier limits sheet (Forman et al., 1999a). Evidence for earlier glacial during the early Holocene (10–8 ka). At a number of events is better delineated on the Eurasian mainland by localities on Franz Josef Land, within 1–2 km of the glacier marginal deposits in north Russia (Markhida present glacier margin, in situ shells from raised-marine Line) and west Siberia that indicate ice-sheet advance sediments yield 14C ages between 9.7 and 8.3 ka, from the Barents and Kara Seas onto the mainland ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1411 during the Early (c. 100 ka) or Middle (60–70 ka) are close to isostatic equilibrium at present (Table 1). Weichselian (Astakhov, 1998; Forman et al., 1999b; The uplift rate constant (k) for Franz Josef Land and Mangerud et al., 1999; Svendsen et al., 1999), though eastern Svalbard is relatively uniform yielding mean there is also evidence for northerly ice flow into the Kara values of 3.2 Â 10À4/yr and 3.4 Â 10À4/yr for the past Sea from mainland Russia (Forman et al., 2002; 12,000 calendar years (Table 1). The resultant average Lokrantz et al., 2003). half-life of uplift is approximately 2000 years, which is This assessment of the pattern of postglacial emer- similar to values for northern Canada (Andrews, 1968; gence for the Barents Sea places a maximum Late Dyke et al., 1991) and Fennoscandinavia (Bakkelid, Weichselian ice sheet load over the northern Barents Sea 1986; Weihe, 1996). The present estimated rate of and eastern Svalbard. The emergence data from Franz uplift for Franz Josef Land is 1.170.9 mm/yr, with an Josef Land indicate substantially less isostatic compen- inferred 3–2 m of uplift remaining (Table 1). The sation than eastern Svalbard (Salvigsen, 1981; Salvigsen inferred present rate of uplift on eastern Svalbard is and Mangerud, 1991; Bondevik et al., 1995). Observa- similar at 1.170.3 mm/year, with 1.5–5.5 m of tions of a low (10–15 m aht) and young (B6000 14Cyr isostasy projected in to the future. Kongs^ya, Aagard- BP) postglacial marine limit on Novaya Zemlya (For- bukta on eastern Spitsbergen, and localities on Bare- man et al., 1995, 1999a; Zeeberg et al., 2001) confines the nt^ya and on Edge^ya have the greatest inferred maximum ice sheet load to the northern and western remaining emergence (3.4–5.5 m) and the present Barents Sea. The pattern of glacio-isostasy is incon- uplift rates (1.2–1.6 mm/yr), which is consistent with sistent with a dominant ice sheet load modeled over maximum Late Weichselian glacier loads over the Novaya Zemlya and the Kara Sea (Peltier, 1994, 1996). Barents Sea and eastern Svalbard (Salvigsen, 1981; The southern limit of maximum isostatic rebound in the Forman, 1990; Forman et al., 1995, 1997; Landvik Barents Sea is more difficult to constrain. However, et al., 1998). there is no evidence for northerly deflection of post- The estimated contemporary, maximum uplift rates of glacial isobases on Fennoscandinavia or the Kola 0.7–1.6 mm/yr for eastern Svalbard and Franz Josef Peninsula (M^ller, 1986; Snyder et al., 1996) indicating Land are consistent with the closest tide gauge a diminished ice-sheet load and/or early deglaciation of measurements on northern Novaya Zemlya, Russkaya the southern Barents Sea. Glacio-isostatic response was Gavan (Emery and Aubrey 1991, p. 114). Sea level even more modest in the southern Barents Sea with measurements for this locality in the northern Barents marine limits registered at o10 m on southern Novaya Sea over the past 40 years yield a land uplift rate of Zemlya and Kolguev Island (Forman et al., 1995), zero 2 mm/yr. In contrast, predicted uplift residuals of 3– emergence on Bear Island (Salvigsen and Slettemark, 8 mm/yr (Peltier, 1996; M2 model) are at odds with the 1995) and Vaygach Island (Zeeberg et al., 2001) and observed current uplift rates of 0.7–2 mm/yr, reflecting postglacial submergence of the Pechora lowland coast the rheological response from a modelled 2-to-2.5-km (Tveranger et al., 1995). thick Late Weichselian ice-sheet over the Barents and Modeling the course of uplift in the Barents Sea Kara seas, (Peltier, 1994, 1996). provides insight into eustatic and isostatic controls on The sea-level curve from Barbados currently provides the course of postglacial relative sea-level. An exponen- the best approximation of the course of global sea level tial function (U=Cekt; where U=uplift, C=remnant during the last deglaciation (Fairbanks, 1989). However, uplift, k=rate constant and t=time), provides a first- uncertainty remains on directly applying sea-level order approximation for the form of postglacial uplift estimates from Barbados to the Barents Sea because of for many areas that sustained 1000+m-thick ice sheets imprecise estimates on the progression of the geoid in the Late Weichselian (Andrews, 1968, 1970; Bakkelid, during deglaciation and gravitational effects on sea level 1986; Forman et al., 1997). A similar formulation is used by adjacent ice sheets (e.g. Morner,. 1978; Anderson, to model uplift for Franz Josef Land, eastern Svalbard 1984; Fjeldskaar, 1994). To minimize uncertainties of and Novaya Zemlya, which yielded highly correlated fits applying an equatorial sea level record to the Barents (R2=>0.90; Table 1). Calculations using emergence Sea, the derivative of the Barbados sea-level curve data spanning the past 10 ka are corrected to reflect total (Fairbanks, 1989) is presented as a negative rate uplift by adding the estimated rise in global sea-level compared to the modelled isostatic response (Fig. 12). during this interval (Fairbanks, 1989). It is assumed that The average rates of eustatic sea-level rise and isostatic global sea level is stable after 6 ka (Kidson, 1982) and adjustment are computed in 1000 14C year increments the total sea level rise is B55 m after 10.5 ka (Fairbanks, for the past 10 ka (Fig. 12). The difference between the 1989; Peltier, 1994). To assess present rates of uplift and rate of eustatic rise and isostatic compensation yields a uplift half-lives, the radiocarbon chronology for uplift is predicted emergence rate/ka. This predicted emergence converted to calendric time (Stuiver et al., 1998). rate is then compared to the measured emergence rate Exponential fit of 14C-corrected uplift data for Franz for Hooker and Scot Keltie islands and Koldewey Josef Land and east Svalbard indicate that these areas Island, southern Franz Josef Land (Forman et al., 1996, ARTICLE IN PRESS 1412 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Fig. 12. Plot of the rate of sea-level change for 1000 14C yr BP intervals for the past 11,000 yr. Changes in eustasy derived from Fairbanks (1989). Modeled uplift rate derived from exponential fit of uplift data (Forman et al., 1997). Rate of modelled emergence is derived by subtracting rate of eustasy from rate of modelled uplift. Measured emergence rate is from empirically derived relative sea-level curve for Hooker and Scott Keltie islands (Forman et al., 1996).

1997) to evaluate the interplay between eustasy and measurements, whereas solid-Earth models are forced isostasy in the Barents Sea (Fig. 12). by rebound records. Like solid-Earth models, ice-sheet The measured emergence rate for Hooker and Scott models also assist in the interpretation of uplift records Keltie Islands agrees well with modeled rates from the by providing information in regions where data are past 7 ka (Fig. 12), consistent with the primacy of glacio- absent, and for extending uplift rates backwards in time. isostatic adjustment in the middle and late Holocene for One argument against the use of ice-sheet models for controlling the course of relative sealevel in the Barents this purpose is that their solid-Earth component is basic. Sea. However, prior to 7 ka there is a noticeable However, a model inter-comparison exercise has re- discrepancy, particularly on Hooker and Scott Keltie vealed little difference between the results of sophisti- islands, with measured emergence rates lower than those cated Earth rheology models and some much simpler predicted (Fig. 12). This lower initial emergence rate on models (Le Meur and Huybrechts, 1996). In particular, Franz Josef Land is reflected as a diachronous marine simple models are capable of determining uplift rates limit dated between 10.4 and 6 ka, and previously and patterns across regions that have experienced denoted as a transgression (Naslund. et al., 1994)oran deglaciation, though they are less good at determining arrest with fall in relative sea level (Forman et al., 1996). uplift distal to formerly glaciated terrain. It is unlikely that the lower measured rates of emergence Siegert et al. (1999) used an ice-sheet model to before 7 ka reflect glacier reloading, with outlet glaciers understand the glacial history of the Eurasian Arctic. at or behind present position by the early Holocene As the model ran, the topographic grid, over which the (Lubinski et al., 1999). Alternatively, the reflooding of ice sheet was constructed, was continually adjusted to the Barents Sea after deglaciation, c. 13–10 ka may be a account for ice-loading of the crust through a glacial sufficient load to dampen glacio-isostatic compensation. cycle following the isostasy method developed in Oerle- The average present depth of the Barents Sea is 230 m mans and van der Veen (1984). In this method, the total and at c. 10–9 ka the western and central portions were deflection of the lithosphere can be approximated as the approximately 150–50 m deeper because of down warp- sum of the deflections caused by discrete loads in each ing from prior ice-sheet loading. The inferred water load cell. The lithosphere is allowed to approach equilibrium in the Barents Sea c. 10 ka may be equivalent to 20–10% by an exponential decay. In each model year the of the modelled ice-sheet load during the glacial lithosphere is adjusted by 1/f times the distance to maximum (Lambeck, 1995) and would dampen the equilibrium. The value of f, a characteristic time initial rate of emergence (Forman et al., 1997). constant governing the rate at which isostatic adjust- ment occurs, is taken as 3000 years, which is compatible with that determined by Fjeldskaar (1994) from 9. Comparison of modeland data or glacialisostasy Scandinavia. The ice-sheet was forced to decay, through enhanced The glacial history hypothesised from analysis of rates of iceberg calving, from geologically-derived limits raised beaches can be tested using numerical ice-sheet at the LGM (Svendsen et al., 1999; Fig. 13). The pattern models. Such models differ from solid-Earth models in of ice decay was matched to further ice sheet limits at that uplift rate calculations are made independent of 15,000 and 12,000 cal. yr (Landvik et al., 1998). The ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1413

Fig. 13. Ice sheet thickness at (a) 14,000 cal. yr ago, (b) 13,000 cal. yr ago, (c) 12,000 cal. yr ago, (d) 11,000 cal. yr ago. Contours are in meters (Siegert and Dowdeswell, 2002). result was a time-dependent view of ice sheet decay to Franz Josef Land. The contours are concentric about across the Eurasian Arctic (Siegert and Dowdeswell, the central Barents Sea, which is consistent with uplift 2002). isobases (Fig. 6). As ice decay continues, this centre At the LGM the model predicts the ice sheet to be migrates northwards such that by 9 cal. ka (8.1 14Cka)it over 2.5 km thick across Scandinavia, around 1 km in is located to the south of Kong Karls Land (and to the the Barents Sea, and less than 300 m thick to the east west of Hopen) in the northwestern Barents Sea. over the Kara Sea (Fig. 13). Ice decay began within the Second, Severnaya Zemlya and the Kara Sea experi- deep bathymetric troughs of the Barents Sea. In enced very little uplift, and the Taymyr Peninsula particular ice calved embayments existed within the virtually none. Third, Bear Island, to the north of the Bear Island Trough in the western Barents Sea, and the Bear Island Trough on the western margin of the Franz Victoria Trough to the north, west of Franz Josef Barents Sea, experienced quite low uplift rates during Land (Fig. 14). By 13 cal. ka ago, the model suggests deglaciation (o20 m 1000 yrÀ1 at 11 ka), and virtually that the Bear Island embayment increased in size to no uplift subsequent to ice decay. Fourth, at 11 cal. ka occupy the majority of the southern Barents Sea. (B9.7 14C ka) the model predicts an uplift rate gradient Following this, the Franz Victoria embayment grew from north to south across Novaya Zemlya. In the north southwards, thus separating the ice cap over Svalbard the rate is quite low (close to zero at the northern and the northwest Barents Sea from ice over Novaya extreme of the island), whereas in the southwest it is Zemlya and Scandinavia. By 11 cal. ka ago, small ice around 100 m 1000 yrÀ1. At this time, however, the caps over Svalbard and the southernmost Kara Sea are model predicts that the island to be covered by ice, all that was left of the former marine ice sheet. Across which is in agreement with limited glacial geologic Scandinavia, however, the ice was as thick as 2 km. This observations (Forman et al., 1999a, b). Subsequent to land-based ice quickly decayed such that by 9 ka very deglaciation of Novaya Zemlya, at 10 ka (B9 14C ka), little of the Eurasian ice sheet remained. the gradient of uplift rates is removed, such that uplift There are four main characteristics of modelled bed rates are between 20 and 40 m 1000 yrÀ1 across the bulk uplift associated with the decay of ice within the of the island. This rate of uplift appears excessive with Eurasian Arctic (Fig. 14). First, contours depicting the actual rates of 1–4 m 1000 yrÀ1 for 6–5 cal. ka (Fig. 11) rate of uplift at 11 ka (B9.7 14C ka) can be traced from and a marine limit of 10–14 m aht for northern Novaya Svalbard across the northern margin of the Barents Sea Zemlya. ARTICLE IN PRESS 1414 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Fig. 14. Rate of bedrock uplift at (a,b) 11,000 cal. yr ago, (c,d) 10,000 yr ago and (e,f) 9000 yr ago. Note that (a), (c) and (e) show contours in 20 m/ 1000 yr up to 100 m/1000 yr and (b), (d) and (f) display contours at 100 m/1000 yr-intervals (Siegert and Dowdeswell, 2002).

10. Conclusions definition, particularly on Svensk^ya, where the highest postglacial marine limit of 120 m+ has been measured The pattern for post-glacial emergence is particularly (Salvigsen, 1981). The glacio-isostatic signature for well constrained for Spitsbergen, Edge^ya and Bare- Franz Josef Land is incomplete with many areas to the nts^ya, but other islands of the archipelago, like north and east remaining largely unstudied Nordaustlandet, have sparse data coverage. The area (Forman et al., 1997). The glacial history of much of of maximum uplift on eastern Svalbard needs better northern and southern Novaya Zemlya is largely ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1415 unknown and additional studies are needed to Zemlya may not have achieved equilibrium reflecting an confirm the modest uplift associated with the last ice sheet loading hemicycle o8000 yr, an important deglacial hemicycle (Forman et al., 1999a, b; Zeeberg consideration for refining Earth rheology-based ice sheet et al., 2001). models. There is clear evidence for early deglaciation of northwestern Spitsbergen by c. 13 ka ago, which results in a variable relative sea level response with transgres- sive and regressive events, compared to deglaciation Acknowledgements at c. 10.5–10 ka for eastern Svalbard where uplift is essentially exponential. Maximum isostatic compensa- This research is supported by National Science tion of >80 m aht is registered on Kongs^ya and Foundation awards DPP-9001471, OPP-9222972 and adjacent eastern Svalbard and these areas and the OPP-9223493, and OPP-9796024 and Office of Naval adjacent Barents Sea are inferred to have sustained the Research contract N00014-92-M-0170 and was under- greatest ice sheet loads (Lambeck, 1995). Emergence taken in cooperation with Leonid Polyak (Ohio State isobases are deflected around Isfjord and Van Mijenf- University). We thank the crew of R/V Dalnie Zelentsy jord, Svalbard indicating sustained and a thicker ice for gaining access to Franz Josef Land (1991–1994). The load associated with these bathymetric lows, presumably work of O.! Ingolfsson! was supported by the Swedish as ice streams. Natural Sciences Research Council, Goteborg. Univer- Ice sheet loading is smaller on southern Franz Josef sity and The University Centre on Svalbard (UNIS). We Land than eastern Svalbard, with maximum emergence express our gratitude to Pyotr Boyarsky and the of 49 m aht on Bell Island. Novaya Zemlya exhibits Heritage Institute (Moscow) for providing access to low total emergence of 15–10 m aht and initiated late, Novaya Zemlya (1995, 1998) and Vaygach Island c. 6–5 ka. Modest and late emergence on Novaya (2000). Dmitri Badyukov supported us in the field. Zemlya and Franz Josef Land indicates that these Thanks are also due to George Maat and Henk van areas sustained modest ice sheet loads at the reactive Veen (Stichting Willem Barents, The Netherlands) for northern and eastern margins of the Barents Sea help with logistical arrangements and the Corps Marines ice sheet. The estimated half-life for uplift in the of the Royal Dutch Navy for provision of gear. Barents Sea is approximately 2000 yr. Present uplift Transport in 1998 was aboard R.V. Ivan Petrov (Arch- rates are between 0.5 and 2 mm/yr and emergence is angelsk). near completion with projected future uplift of 1–6 m. Water loading in the glacio-isostatically depressed Barents Sea in the early Holocene (10–7 ka) slowed Appendix A emergence rates. Glacioisostatic equilibrium was probably achieved for eastern Svalbard and islands in Radiocarbon ages on driftwood and associated the Barents Sea. In contrast, areas of western and marine subfossils fromraised beach sequences on Sval- northern Spitsbergen, Franz Josef Land and Novaya bard, Norway (Table 2).

Table 2 The Radiocarbon ages on driftwood and associated marine subfossils are presented in Table 2

Dated material Shoreline Laboratory 14C d13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Blomsletta/Billefjorden, Spitsbergen: marine limit B90+m aht Mytilus edulis valves 5.8 3370790 U-126 Feyling-Hansen and Olsson (1959) and Olsson (1960) Mollusc fragments 8.0 5630765 SI-4307 Pew! e! et al. (1982) Shells from Arstarte terrace 17 75957110 U-130 Feyling-Hansen and Olsson (1959) Shell valves of Mytilus edulis 19.5 6000780 T-4628 Salvigsen (1984) Mya truncata samples 21.2 8480770 SI-4306 Pew! e! et al. (1982) Mya truncata samples 31.3 9340775 SI-4308 Pew! e! et al. (1982) Mixed shells 42 88707200 U-124 Feyling-Hansen and Olsson (1959) Mixed shells 50.7 95407140 U-128 Feyling-Hansen and Olsson (1959) Mixed shells 56 94007150 U-132 Feyling-Hansen and Olsson (1959) Driftwood, Larix occidentalis 65 10,0307140 Salvigsen (1984) ARTICLE IN PRESS 1416 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Table 2 (continued)

Dated material Shoreline Laboratory 14C d13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Brøggerhalvøya, western Spitsbergen: marine limit 4671 m aht Whale vertebrae partially buried in 4 92307340 À17.0 GX-9908 Forman et al. (1987) raised beach Shell fragments from soil pit in raised 5 99607110 +2.6 GX-9894 Forman et al. (1987) beach Whale vertebrae partially buried in 8 98007370Ã À16.8 GX-9893 Forman et al. (1987) raised beach Whale vertebrae partially buried in 14 93657280Ã À16.8 GX-9892 Forman et al. (1987) raised beach Paired valves of Mya truncata from 15+ 10,620790 02 DIC-3122 Forman et al. (1987) sublittoral sands Paired valves of Hiatella arctica from 20+ 99507315 02 GX-8590 Miller (1982) sublittoral sands Whale rib embedded in raised beach 23 99207315Ã À17.0 GX-9891 Forman et al. (1987) Unidentified bone fragment 27 6207135Ã À15.6 GX-10106 Forman et al. (1987) Whale ribpartially buriedin raised 30 96057155Ã À16.3 GX-10730 Forman et al. (1987) beach Unidentified bone fragment 36 22,2207600Ã À16.8 GX-10105 Forman et al. (1987) Whale ribfrom crest of 37 m raised 37 10,8807170Ã À15.0 GX-10731 Forman et al. (1987) beach Whale ribfrom crest of 37 m raised 37 11,7607430 À15.2 GX-9990 Forman et al. (1987) beach Whale ribfrom crest of 37 m raised 37 11,8007180 À20.0 I-13793 Forman et al. (1987) beach (sub sample of GX-9990) Whale vertebrae behind marine limit 46 >36,000 À15.7 GX-9907 Forman et al. (1987) Whale ribbehindmarine limit 46 >35,710 75070– À15.7 GX-9907 Forman et al. (1987) 3080

Mitrahalvøya, western Spitsbergen: marine limit 2072 m aht Whale vertebrae partially buried in 225775 À15.5 GX-10771 Forman (1990) raised beach Whale ribpartially buriedin raised 5 94157155 À16.6 GX-10775 Forman (1990) beach Whale ribpartially buriedin raised 7 95057155 À16.8 GX-10773 Forman (1990) beach Whale ribpartially buriedin raised 4 96007160 À16.5 GX-10778 Forman (1990) beach Whale ribpartially buriedin raised 10 98407160 À16.5 GX-10772 Forman (1990) beach Whale cranium buried in raised beach 15 10,3107330 À17.7 GX-10103 Forman (1990) Whale cranium in beach gravels at 20 12,9607190 À17.4 B-10968 Forman et al. (1987) marine limit

Tønsneset, western Spitsbergen Whalebone behind modern storm 5 59007210 À16.6 GX-9899 Forman et al. (1987) beach Shell and barnacle fragments from 10 10,0657170 +1.7 GX-10104 Forman et al. (1987) raised beach Shell from raised beach surface 10 91857120a Tln-249 Punning et al. (1978)

Daudmannsøyra, western Spitsbergen: marine limit 4872 m aht Larch log buried in raised beach 5.5 5590790 À252 DIC-2902 Forman (1990) gravels In situ Mytilus edulis paired valves 4 60307200 À0.4 GX-10037 Forman (1990) Whale ribpartially buriedin raised 10 88107140 À17.9 GX-10777 Forman (1990) beach gravels Whale vertebrae partially buried in 14 90407165 À16.8 GX-10776 Forman (1990) raised beach gravels Whale vertebrae partially buried in 30 92957160 À16.0 GX-10593 Forman (1990) raised beach gravels Whale rib embedded in raised beach 38 93557170 À16.6 GX-10591 Forman (1990) ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1417

Table 2 (continued)

Dated material Shoreline Laboratory 14C d13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Whale vertebrae partially buried in 24 94207160 À17.6 GX-10592 Forman (1990) raised beach gravels Whale ribpartially buriedin raised 42 99407310 À14.4 GX-9910 Forman (1990) beach gravels

Southern Prinz Karls Foreland, western Spitsbergen: marine limit 3672 m aht Whale cranium buried in raised beach 3 370780- À15.9 GX-10734 Forman (1990) surface Whale vertebrae on raised beach 4 820780- À15.9 GX-10735 Forman (1990) Whale ribpartially embedded into 3 49257100 À15.9 GX-10732 Forman (1990) raised beach In situ Mytilus edulis paired valves 5 8940790 02 DIC-3054 Forman (1990) from raised beach Paired valves Mya truncata from 10 9420790 02 DIC-3052 Forman (1990) raised beach Whale jaw bone 10 94107140 À19.2 T-2235 Salvigsen (1977) Whalebone 28 95607130 À16.1 T-2233 Salvigsen (1977) Whale rib partial buried in beach 32 10,4707160 À19.2 I-13794 Forman (1990) gravels Whale jaw bone partial buried in 35 11,2107180 À19.2 I-13795 Forman (1990) beach gravels

Ytterdalen, N. Bellsund western Spitsbergen: marine limit 6472 m aht Whalebone 7.0 4490750 T-5664 Landvik et al. (1987) Whalebone 9.1 5210790 T-5407 Landvik et al. (1987) Seaweed 8.2 61807180 T-5406 Landvik et al. (1987) Whalebone 12.5 77607110 T-6221 Landvik et al. (1987) Driftwood of Picea sp. 10 77707110 T-5271 Landvik et al. (1987) Whalebone 11.1 79507120 T-5665 Landvik et al. (1987) Whalebone 26.2 89107140 T-5408 Landvik et al. (1987) Balanus sp. 24 90107130 T-5663 Landvik et al. (1987) Fragments of Mytilus edulis from 13.8 90307100 T-5662 Landvik et al. (1987) raised beach surface Whalebone 29.6 91307130 T-5409 Landvik et al. (1987) Fragments of Hiatella arctica and >30 10,240770 T-4943 Landvik et al. (1987) Mya truncata from silt Hiatella arctica valves from frost 50.9 10,6007130 T-5410 Landvik et al. (1987) sorted sediments Fragments of Hiatella arctica and 55.6 10,8407110 T-5995 Landvik et al. (1987) Mya truncata from gravels Fragments of Hiatella arctica and 50.6 11,0207110 T-4865 Landvik et al. (1987) Mya truncata from surface

Wedel Jarlsberg Land, S. Bellsund, western Spitsbergen: marine limit 55–60 m aht Shell fragment from beach gravels 50.5 11,9107145 02 Ua-1081 Salvigsen et al. (1991) that rise to marine limit Fragment of Mya truncata or Hiatella >48 11,3557160 02 Ua-1082 Salvigsen et al. (1991) arctica from silt Small bone, probably whale and 51.3 94707160 À14.6 T-7669 Salvigsen et al. (1991) elevationally displaced Large whale vertebrae buried in 25.3 91807130 À15.6 T-7671 Salvigsen et al. (1991) beach gravels Log of Larix sibirica embedded in 10.8 87607120 À26.12 T-7672 Salvigsen et al. (1991) permafrost/gravels Whale jaw from raised beach 10 89607120 À18.8 T-1829 Salvigsen (1977) Large whale cranium within beach 6.7 59707100 À14.4 T-76701 Salvigsen et al. (1991) gravels 10-m long log of Larix occidentalis on 6.0 1100780 02 T-7672 Salvigsen et al. (1991) raised beach ARTICLE IN PRESS 1418 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Table 2 (continued)

Dated material Shoreline Laboratory 14C d13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Mosselbukta, northern Spitsbergen: marine limit 65 þ m aht Driftwood Picea sp. 5 75307100 T-3454 Salvigsen and Østerholm (1982) Shell valves of Mya truncata 35 9,3607110 T-3734 Salvigsen and Østerholm (1982) Shell valves of Mya truncata and 65 10,6607100 T-3735 Salvigsen and Østerholm (1982) Hiatella arctica

Grahuken( , northern Spitsbergen: marine limit 40 þ m aht Whale cranium 6 8830770 T-3097 Salvigsen and Østerholm (1982) Shell valves of Mytilus edulis 8 93607110 T-3098 Salvigsen and Østerholm (1982) Shell valves of Hiatella arctica 41 10,9207120 T-3099 Salvigsen and Østerholm (1982)

Reinsderflya. northern Spitsbergen: marine limit 2572 m aht Whale cranium 5 9160770 T-2838 Salvigsen and Østerholm (1982) Whale ribon raised beach 19 9330 790 T-2703 Salvigsen and Østerholm (1982) Whale ribon raised beach 23 9850 7135 À17.0 GX-11294 Lehman (1989) Whale ribfrom sublittoral sands 9.5(15) 9130 7210 À17.2 GX-10685 Lehman (1989) In situ paired valves of Mytilus edulis 5 9015780 À19 DIC-3076 Lehman (1989) in beach gravels

Woodfjord, northern Spitsbergen: marine limit 74 m aht Paired valves of Mytilus edulis 5.20 5970750 2.3 UtC-10089 Bruckner. et al. (2002) Duplicate of UtC-10089 5.20 6012744 0.6 Hd-20823 Bruckner. et al. (2002) Shell debris from raised beach ridge 2 6597755 2.9 Hd-20946 Bruckner. et al. (2002) Shell debris, mostly Mytilus edulis 5.20 9370757 1.3 UtC-10142 Bruckner. et al. (2002) from beach ridge Mostly Balnus sp. debris from beach 7.50 9377749 0.3 UtC-10140 Bruckner. et al. (2002) ridge Paired valves of Mya truncata from 11.60 9130760 0.9 UtC-10138 Bruckner. et al. (2002) beach ridge Mytilus edulis from beach ridge 4.50 8842775 0.9 Hd-20789 Bruckner. et al. (2002) Whale rib buried in beach ridge 5.20 8797775 À17.9 Hd-20989 Bruckner. et al. (2002) Balnus sp. debris from beach ridge 11.60 9395766 1.6 Hd-20872 Bruckner. et al. (2002) C in living position from beach ridge 20.50 9459751 1.8 Hd-20891 Bruckner. et al. (2002) Duplicate of Hd-20891 20.50 9462750 1.5 UtC-10084 Bruckner. et al. (2002) Shell debris from raised beach ridge 24.20 9490760 1.3 UtC-10147 Bruckner. et al. (2002) Paired Mya truncata valves from 22.70 9520760 0.8 UtC-10083 Bruckner. et al. (2002) raised beach Shell debris of Mya truncata from 22.70 96877102 2.3 Hd-20806 Bruckner. et al. (2002) raised beach Paired Mya truncata valves from 17.80 9540772 1.8 Hd-21035 Bruckner. et al. (2002) raised beach Mya truncata in living position in B17 9590750 1.1 UtC-10152 Bruckner. et al. (2002) homogeneous sand Duplicate of UtC-10152 B17 9660781 1.5 Hd-20824 Bruckner. et al. (2002) Paired Mya truncata valves from 22.70 9591777 1.8 Hd-20822 Bruckner. et al. (2002) raised beach Duplicate of Hd-20822 22.70 9639781 1.5 Hd-22790 Bruckner. et al. (2002) Shell debris from raised beach ridge 20.00 9618748 2.5 UtC-10095 Bruckner. et al. (2002) Shell debris from raised beach ridge 26 9658765 1.6 Hd-21014 Bruckner. et al. (2002) Paired Hiatella arctica valves from >33 9806743 1.2 UtC-10154 Bruckner. et al. (2002) sublittoral sand Single shell valve from raised beach 33 10,443744 À0.4 UtC-10155 Bruckner. et al. (2002) (same as Hd-20988) Shell debris from raised beach 33 9825786 1.2 Hd-20993 Bruckner. et al. (2002) Shell debris from raised beach (same 34 10,659791 1.8 Hd-20988 Bruckner. et al. (2002) as UtC-10153) Hiatella arctica from raised beach 34 9970760 1.7 UtC-10146 Bruckner. et al. (2002) Mya truncata from raised beach 30 10,041766 1.6 Hd-20998 Bruckner. et al. (2002) Mya truncata from raised beach 33 10,170760 1.8 UtC-10153 Bruckner. et al. (2002) Shell debris from raised beach 44 11,000760 1.7 UtC-10145 Bruckner. et al. (2002) Mya truncata from raised beach 55.20 11,040760 1.5 UtC-10144 Bruckner. et al. (2002) ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1419

Table 2 (continued)

Dated material Shoreline Laboratory 14C d13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Shell debris from sublitoral sands at 41 11,087757 1.5 Hd-20867 Bruckner. et al. (2002) base of beach ridge Shell debris from fjord terrace B40 11,091779 1.8 Hd-20807 Bruckner. et al. (2002) disturbed by solifluction Mya truncata from marine sediments >40.90 11,115775 1.5 Hd-20781 Bruckner. et al. (2002) on top of till Mya truncata from raised beach 44.10 11,150760 2.1 UtC-10143 Bruckner. et al. (2002) Paired valves of juvenile Mya 69.50 11,530760 1.5 UtC-10141 Bruckner. et al. (2002) truncata from highest terrace

Bohemanflya and Erdmannflya, Isfjord, Spitsbergen: marine limit 65.571 m aht Whale cranium 3.5 5,150780 T-6289 Salvigsen et al. (1990) Shell valves of Mytilus edulis 8.0 7680790 – T-6283 Salvigsen et al. (1990) Shell valves of Mytilus edulis 10 7690780 Lu-2139 Salvigsen et al. (1990) Shell valves of Mya truncata 7.0 79307100 T-8629 Salvigsen et al. (1990) Shell valves of Mytilus edulis 11.6 80607100 T-6288 Salvigsen et al. (1990) Shell valves of Mytilus edulis 5.0 8210790 T-6284 Salvigsen et al. (1990) Shell valves of Modiolus modiolus 6.5 8670790 T-6235 Salvigsen et al. (1990) Shell valves of Mytilus edulis 16 89707110 T-6285 Salvigsen et al. (1990) Shell valves of Mya truncata 18–20 9190790 Lu-2138 Salvigsen et al. (1990) Shell valves of Mya truncata and 41 95007100 T-6286 Salvigsen et al. (1990) Hiatella arctica Shell valves of Hiatella arctica 20 9510790 Lu-2364 Salvigsen et al. (1990) Shell valves of Hiatella arctica 29 96807110 T-6282 Salvigsen et al. (1990) Shell fragments 47 97207110 T-6287 Salvigsen et al. (1990) Whale jaw bone 35 11,2107180 I-13795 Salvigsen et al. (1990)

Agardhbukta area, eastern Spitsbergen: marine limit 5071 m aht 13-m long log of Pinus silvestris 1.5 810780 À26.12 T-4941 Salvigsen and Mangerud (1991) 5.7-m long lower whale jaw bone in 3.0 800770 À15.9 T-5127 Salvigsen and Mangerud (1991) beach gravels 2-m long log of Larix gmelini in beach 15.0 46907100 À26.12 T-4942 Salvigsen and Mangerud (1991) gravels Whale baleen from beach gravels 16 49907105 À17.0 T-5128 Salvigsen and Mangerud (1991) Shell fragments with Mya truncata 8 53307100 À1.0d T-5125 Salvigsen and Mangerud (1991) and Balanus sp. 5-m long log of Larix sibirica buried 20.5 6450770 À26.12 T-4939 Salvigsen and Mangerud (1991) in beach gravels Whale rib embedded in beach gravels 24.0 6810+110 À15.4 T-5126 Salvigsen and Mangerud (1991) Shell fragments of Mya truncata and 36.5 90407140 1.6 T-4938 Salvigsen and Mangerud (1991) Balanus sp. 2-m long whale ribimbeddedinto 50 98707140 À26.3 T-4937 Salvigsen and Mangerud (1991) raised beach

Hornsund, southern Spitsbergen: marine limit B25 m aht 10-m long log on surface 5.5 1080770 À23.7 U-619 Birkenmajer and Olsson (1970) Whale jaw bone 5.5 680770 À19.5 U-2048 Birkenmajer and Olsson (1970) Shell valves of Mya truncata, A. 5.5 88707180 À2.1 U-2079 Birkenmajer and Olsson (1970) borealis and C. islandica Shell fragments of Mya truncata and 7.5 91807110 +0.2 U-665 Birkenmajer and Olsson (1970) Hiatella arctica Shell fragments mostly of Balanus sp. 8.0 6770790 +0.3 U-682 Birkenmajer and Olsson (1970) Whale lower jawbone, 1.9-m long 8.0 89407140 À17.1 U-703 Birkenmajer and Olsson (1970) Another collagen fraction of U-703 8.0 94007230 À18.2 U-2130 Birkenmajer and Olsson (1970) Hiatella arctica from raised beach 20–21 9920790 T-6222 Landvik et al. (1992) gravels

Southern Sørkapp Land, southern Spitsbergen: marine limit 1071 m aht Seaweed (Laminaria sp.) in beach 2 2715785 T-10861 Ziaja and Salvigsen (1995) gravels Whalebone within beach gravels 10 64657105 T-10860 Ziaja and Salvigsen (1995) ARTICLE IN PRESS 1420 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Table 2 (continued)

Dated material Shoreline Laboratory 14C d13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Seaweed (Laminaria sp.) in beach 9.5 6440755 T-10859 Ziaja and Salvigsen (1995) gravels Seaweed (Laminaria sp.) in beach 9.5 65807160 Gd-6583 Wojcik! and Zala (1993) gravels

Kongsøya: marine limit 100+m aht 25-cm diameter log of Larix sp. 2.5 110760 T-3727 Salvigsen (1981) 50-cm diameter log of Populus sp. 4.7 750760 T-3460 Salvigsen (1981) 50-cm diameter log of Pinus sp. 10.3 2150770- T-3728 Salvigsen (1981) 50-cm diameter log of Larix sp. 16.0 3110780 T-3729 Salvigsen (1981) 50-cm diameter log of Larix sp. 17.2 2620770 T-3459 Salvigsen (1981) 50-cm diameter log of Pinus sp. 23.5 3970780 T-3730 Salvigsen (1981) 40-cm diameter log of Larix sp. 27.0 4440+80 T-3726 Salvigsen (1981) 15-cm diameter log of Larix sp. 31.5 5240770 T-3458 Salvigsen (1981) 30-cm diameter log of Larix sp. 36.6 5850770 T-3733 Salvigsen (1981) 15-cm diameter log of Picea sp. 44 6760790 T-3457 Salvigsen (1981) Whalebone 50 76407110 T-3731 Salvigsen (1981) 25-cm diameter log of Picea sp. 58 83707100 T-3456 Salvigsen (1981) Whalebone 88 87407130 T-3907 Salvigsen (1981) 25-cm diameter log of Larix sp. 100 97907120 T-3397 Salvigsen (1981) 25-cm diameter log of Larix sp. 100 9850740 GSC-3039 Salvigsen (1981) (subsample of T-3397)

Hopen: marine limit 60+m aht Driftwood 4.4 12007100 St-2455 Hoppe et al. (1969) Driftwood, 1 m-long log, diameter 24 4.5 800770 St-1958 Hoppe et al. (1969) cm 2.8-m long whale jaw bone in beach 5.3 655770 St-2116 Hoppe et al. (1969) gravels Driftwood, root plate 70-cm long, 8.2 1740770 St-2020 Hoppe et al. (1969) diameter 38–32 cm Whale rib, 165-cm long, diameter 12– 12.5 3670780 St-2120 Hoppe et al. (1969) 20 cm Driftwood, root plate 84-cm long, 12.8 3065775 St-2019 Hoppe et al. (1969) diameter 38–32 cm Driftwood, >2-m long log, diameter 14.8 4010780 St-1959 Hoppe et al. (1969) 24 cm Whale vertebrae 14.8 37857100 St-1958 Hoppe et al. (1969) Whale rib, 1.2-m long, diameter 17.9 4115780 St-2213 Hoppe et al. (1969) 13 cm Driftwood 23.5 5935780 À26.8 St-8606 Zale and Brydsten (1993) Driftwood 27 6100780 À25.1 St-8605 Zale and Brydsten (1993) Driftwood 30.5 6240780 St-2018 Hoppe et al. (1969) Driftwood 48.5 95357120 À27.0 St-8603 Zale and Brydsten (1993) Driftwood, 1.1-m long log 50.6 94357115 St-1960 Hoppe et al. (1969) Driftwood, probably a root, 1.5-m 51.1 95107120 St-2225 Hoppe et al. (1969) long log, diameter 18 cm Driftwood 58 98007130 À27.4 St-8604 Zale and Brydsten (1993)

Kapp Ziehen, Barentsøya: marine limit 88.571.0 m aht 2.1-m long log of Larix gmelini buried 3.8 655750 À24.52 Lu-3542 Bondevik et al. (1995) in sediments 4.0-m long log, 25-cm diameter found 4.8 975760 À24.52 Lu-3385 Bondevik et al. (1995) on surface 1.6-m long log of Pinus cembra 8.9 2835750 À24.52 T-10251 Bondevik et al. (1995) 1.3-nm long log of Picea abies 12 3605770 À24.52 Lu-3543 Bondevik et al. (1995) 2.8-m long log of Picea sp. 13.5 3640790 À24.52 T-10252 Bondevik et al. (1995) 1.3-m long log of Picea mariana 17.2 4475795 À24.52 T-9918 Bondevik et al. (1995) buried in sediments 0.8-m long log root piece of Picea sp. 20.5 4680775 À24.52 T-10253 Bondevik et al. (1995) ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1421

Table 2 (continued)

Dated material Shoreline Laboratory 14C d13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

2.4-m long log of Picea sp. embedded 22.8 5355780 À24.52 LU-3383 Bondevik et al. (1995) in beach ridge 1.8-m long log of Larix sp. in beach 30 6170785 À24.52 T-9917 Bondevik et al. (1995) sediment 1.6-m long log with root plate of 34 72207110 À24.52 T-10254 Bondevik et al. (1995) Pinus cembra Small piece of log with partial root 36.6 6950740 À24.52 T-10981 Bondevik et al. (1995) plate 0.30-m long log buried by 1 m of 36.6 6945750 À24.52 T-10980 Bondevik et al. (1995) beach gravel Paired valves of Hiatella arctica 36.6 6995760 1.02 TUa-690 Bondevik et al. (1995) buried by 1 m beach gravel At least 1.6-m long log of Larix 39.2 78807115 À24.52 T-10255 Bondevik et al. (1995) gmelini buried in sediments At least 1.6-m long log of Pinus 42.9 79057110 À24.52 T-9916 Bondevik et al. (1995) cembra in beach ridge 0.55-m long whale rib50.1 8855 7160 À16.4 T-10257 Bondevik et al. (1995) At least 0.9-m long log of Larix 56.7 8870755 À24.52 T-9915 Bondevik et al. (1995) larcina buried in sediments Piece of Hiatella arctica buried by 63.6 9205785 1.0 TUa-689 Bondevik et al. (1995) 1.4 m beach gravel Two big whale jaw bones buried by 63.5 9135745 À19.8 T-10978 Bondevik et al. (1995) 1.4 m beach gravels 2.0-m long log of Salix sp. buried in 63.5 9105755 À24.52 T-9914 Bondevik et al. (1995) sediments 1.15-m long log of Picea abies buried 70.8 94457110 À24.52 LU-3381 Bondevik et al. (1995) in sediment 1.8-m long log of Larix gmelini buried 79.8 96157110 À24.52 LU-3382 Bondevik et al. (1995) in sediments 1.2-m long log of Picea mariana 80.2 9595770 À24.52 T-10256 Bondevik et al. (1995) buried in sediments 1.3-m long whale jaw bone in river cut 88.5 9585760 À20.6 T-99131 Bondevik et al. (1995) through the ML Redate of T-99131 88.5 9470760 À22.9 T-99131I Bondevik et al. (1995)

Humla, Edgeøya: marine limit 86.871.0 m aht Whale jaw bone 3.2 605755– À17.0 T-10806 Bondevik et al. (1995) At least 4-m long log of Pinus silvistri 3.6 580750 À25.1 T-9891 Bondevik et al. (1995) buried in sediments At least 4.5-m long log of Pinus 5.6 1725745 À23.8 T-9897 Bondevik et al. (1995) cembra Whale cranium part on terrace 7.7 2125765 À16.1 T-9880 Bondevik et al. (1995) surface 3.5-m long log partial buried 11.2 3105745 À24.5 T-9885 Bondevik et al. (1995) 0.7-m long log of Larix sp. in beach 14.6 3765740 À24.7 T-9898 Bondevik et al. (1995) sediment 1.0-m long log of Larix sp. in beach 17.2 4460770 À24.0 T-9886 Bondevik et al. (1995) sediment 1.2-m long log of Pinus silvistri buried 19.8 4555765 À25.7 T-9887 Bondevik et al. (1995) in sediments 4-m long log of Picea sp. or Larix sp. 23.4 5130765 À24.2 T-9893 Bondevik et al. (1995) in beach sediments 3.0-m long log of Larix sp. in beach 27.9 5830760 À24.6 T-9892 Bondevik et al. (1995) sediment 4-m long log of Pinus silvistri buried 30.2 6180755 À23.9 T-9890 Bondevik et al. (1995) in sediments 3–4-m long log of Picea sp. or Larix 31.9 6275765 À23.1 T-9883 Bondevik et al. (1995) sp. in beach sediments Two big whale jaw bones partially 35.5 6670790 À18.2 T-9879 Bondevik et al. (1995) buried by beach gravels 0.9-m long log frozen into ice wedge 43.8 7850785 À25.5 T-9894 Bondevik et al. (1995) ARTICLE IN PRESS 1422 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Table 2 (continued)

Dated material Shoreline Laboratory 14C d13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Near vertical >1 m long log of Larix 47.5 8200765 À24.2 T-9884 Bondevik et al. (1995) sp. in ice wedge At least 4.0-m long log of Larix sp. in 51.4 8725770 À23.5 T-9895 Bondevik et al. (1995) beach sediment 2-m long whale jaw bone 55.1 8750790 À16.6 T-10804 Bondevik et al. (1995) At least 3.2-m long log of Larix sp. in 55.1 8720765 À25.2 T-9896 Bondevik et al. (1995) beach sediment 2 big whalebones, possibly jaws 58.8 89407100 À17.5 T-9878 Bondevik et al. (1995) 2.8-m long log of Larix sp. on surface 61.6 9310770 À23.9 T-9889 Bondevik et al. (1995) 1.3-m long whale rib65 9125 7130 À16.9 T-10803 Bondevik et al. (1995) Log of Picea sp. or Larix sp. in 65 9240755 À25.7 T-9888 Bondevik et al. (1995) sediments Large whale jaw bone within 73.9 9310780 À15.6 T-9877 Bondevik et al. (1995) permafrost 0.75 long log on surface 75.6 96207130 À23.6 T-10133 Bondevik et al. (1995)

Southern Edgeøya: marine limit 90–85 m aht Wood fragment of Populus sp. 75.6 9485780 À27.3 T-9882 Bondevik et al. (1995) Shell fragment found on surface 86.8 98857130 1.0 TUa-400 Bondevik et al. (1995) Whale rib1.9 620 7100 À16.42 St-2873 Bondevik et al. (1995) 4.5-m long log in beach sediments 1.9 6207100 St-2819 Bondevik et al. (1995) Dorsal whale vertebrae 3 11707100 À16.42 St-2698 Bondevik et al. (1995) 7-m long log on raised beach surface 3 12407100 St-2660 Bondevik et al. (1995) 2.5-m long log in beach sediments 6 20157100 St-2523 Bondevik et al. (1995) 30-cm diameter log in beach 14 37257100 St-2521 Bondevik et al. (1995) sediments 6.5-m long log partially in beach 16.5 39557100 St-2522 Bondevik et al. (1995) sediments 15-cm diameter log in beach 20 47607100 St-2484 Bondevik et al. (1995) sediments 2.5-m long log partially in beach 24.5 53007100 St-2519 Bondevik et al. (1995) sediments Dorsal whale vertebrae partially in 34.5 66307100 À16.42 St-2579 Bondevik et al. (1995) beach sediments Well-preserved unidentified 39 77957110 À16.4 St-2590 Bondevik et al. (1995) whalebone 1-m long log partially in beach 39.5 79657100 St-2485 Bondevik et al. (1995) sediments 1.5-m long log in beach sediments 53 92307110 St-2520 Bondevik et al. (1995) Large jaw bone 72 95207125 À16.42 T-9908 Bondevik et al. (1995) Shell fragments on raised beach 75 10,200795 +1.02 TUa-269 Bondevik et al. (1995) surface Large log on slope of raised beach 75 95957110 À25.42 T-9907 Bondevik et al. (1995) surface at 75 m aht

Diskobukta, western Edgeøya: marine limit 85.1+m aht 11-m long log partially in beach 3 1270775 À23.7 T-10135 Bondevik et al. (1995) sediments 5-m long log of Larix sp. on surface 4.6 1715775 À23.3 T-10136 Bondevik et al. (1995) 2.1-m long log on raised beach 12.6 3730790 À24.8 T-10142 Bondevik et al. (1995) surface Small log of Larix sp. on surface 15.6 4130790 À24.2 T-10141 Bondevik et al. (1995) 3-m long log of Larix sp. on surface 25.1 6020760 À24.2 T-10137 Bondevik et al. (1995) 1.7-m long log of Picea sp. or Larix 26.6 5930755 À24.9 T-10139 Bondevik et al. (1995) sp. on surface 2 shell valves of Mytilus edulis 26.8 58357125 +0.5 T-9920 Bondevik et al. (1995) 2.7-m long log of Larix sp. on surface 33.3 6770760 À23.5 T-10140 Bondevik et al. (1995) Paired valves of Mytilus edulis 2m 35.4 71757110 +0.5 T-9922 Bondevik et al. (1995) below surface At least a 4-m long log partially 35.4 7255765 À24.6 T-10807 Bondevik et al. (1995) buried in beach gravels ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1423

Table 2 (continued)

Dated material Shoreline Laboratory 14C d13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Large well preserved whalebone on 35.9 70507115 À16 T-10805 Bondevik et al. (1995) surface Short log of Picea sp. or Larix sp. on 36.8 75507115 À25.2 T-10138 Bondevik et al. (1995) surface Paired valves of Mytilus edulis 3.5 m 38 87557125 À0.2 T-9919 Bondevik et al. (1995) below surface Small wood stick from T-9919 38 8615760 À24.5 TUa-691 Bondevik et al. (1995) location 1.2-m long whale ribbone 43.2 8130 770 À17.6 T-10044 Bondevik et al. (1995) 0.25-m long log of Picea sp. 2.5 m 48.9 93457130 À25.4 T-10134 Bondevik et al. (1995) below surface 3.1-m long log of Larix sp. in beach 66 9380745 À24.6 T-10043 Bondevik et al. (1995) gravels 2-m long whale jaw bone 67.8 93357105 À20.3 T-10045 Bondevik et al. (1995) Shell fragment from section near the 77.6 10,015775 +1.7 TUa-338 Bondevik et al. (1995) marine limit Shell fragment likeTUa-338 77.6 9565780 +1 TUa-627 Bondevik et al. (1995)

Svartknausflya, southern Nordaustlandet: marine limit 70+m aht 50-cm diameter log of Larix sp. 2.7 1570770 T-2512 Salvigsen (1978) 25-cm diameter log of Pinus sp. 4.5 2600770 À24.5 T-2692 Salvigsen (1978) 15-cm diameter log of Larix sp. 7.7 3520770 T-2511 Salvigsen (1978) 30-cm diameter log of Larix sp. 10.5 40207100 À24.4 T-2693 Salvigsen (1978) 15-cm diameter log of Salix sp. 12.2 4100790- À27.1 T-2694 Salvigsen (1978) 30-cm diameter log of Picea sp. 14.7 4650790- À27.1 T-2395 Salvigsen (1978) 30-cm diameter log of Larix sp. 16.0 4560780- T-2396 Salvigsen (1978) 30-cm diameter log of Larix sp. 16.4 4970760- À25.9 T-2699 Salvigsen (1978) Whalebone 19.2 5740790 À17.6 T-2510 Salvigsen (1978) 0.5-m long conifer log on raised beach 23.1 6270790 À24.6 T-2698 Salvigsen (1978) surface 45-cm diameter log of Larix sp. 25.1 5850790 T-2509 Salvigsen (1978) 30-cm diameter log of Larix sp. 31.4 74407110 T-2508 Salvigsen (1978) 15-cm diameter log of Salix sp. 36.8 81507100 T-2507 Salvigsen (1978) 40-cm diameter log of Larix sp. 41.8 82007110 T-2506 Salvigsen (1978) 35-cm diameter log of Larix sp. 43.7 87707120 À26.0 T-2695 Salvigsen (1978) 20-cm diameter log of Picea sp. 46.3 88907130 À26.7 T-2696 Salvigsen (1978) 30-cm diameter log of Larix sp. 487 87807110 T-2505 Salvigsen (1978) 25-cm diameter log of Larix sp. 51.8 88007100 T-2504 Salvigsen (1978) Piece driftwood of Larix sp. 52.8 9130780 À26.4 T-2697 Salvigsen (1978) Whalebone 60.7 96407140 À18.5 T-2502 Salvigsen (1978) 8-cm diameter log of Salix sp. 65.5 9550780 T-2696 Salvigsen (1978) Whale vertebrae 70 97007120 À17.0 T-2394 Salvigsen (1978) 20-cm diameter log of Picea sp. 89.9 >46,600 T-2393 Salvigsen (1978)

Lady Franklin Fjord, northern Nordaustlandet: marine limit >50+m aht Driftwood 2.0 67807100 U-33 Blake (1961a,b) Driftwood 6.2 69007110 U-112 Blake (1961a,b) Whalebone 7.5 63807150 U-110 Blake (1961a,b) Driftwood 7.6 62007100 U-107 Blake (1961a,b) Driftwood 8 67407110 U-111 Blake (1961a,b) Mostly Hiatella arctica shells 8.5 91007130 U-120 Blake (1961a,b) Driftwood 8.8 64907110 U-36 Blake (1961a,b) Mostly Mytilus edulis shells 9 86307190 U-173 Blake (1961a,b) Mostly Hiatella arctica shells 9 92907130 U-162 Blake (1961a,b) Driftwood 9.0 66507110 U-116 Blake (1961a,b) Driftwood 9.8 4020790 U-34 Blake (1961a,b) Driftwood 11.3 75007150 U-175 Blake (1961a,b) Driftwood 12.8 78307120 U-38 Blake (1961a,b) Whalebone 17.6 85307180 U-115 Blake (1961a,b) Mostly Hiatella arctica shells 22 92207130 U-179 Blake (1961a,b) Mostly Mya truncata shells 31 93907130 U-95 Blake (1961a,b) ARTICLE IN PRESS 1424 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Table 2 (continued)

Dated material Shoreline Laboratory 14C d13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Driftwood 36.5 92707130 U-70 Blake (1961a,b) Mostly Hiatella arctica shells 44 92007120 U-166 Blake (1961a,b) Phippsøya, Sjuøne, northern Svalbard: marine limit 2271 m aht >0.75-m long log embedded in raised 3 57257115 À24.3 GX-22381 Forman and Ingolfsson! (2000) beach gravel Cranium bone from whale skull, 4 54857110 À19.3 GX-22380 Forman and Ingolfsson! (2000) collagen fraction Paired Hiatella arctica from littoral 5 8970760 À19.3 GX-22387 Forman and Ingolfsson! (2000) gravels 3.5-m long log embedded in raised 6 62257115 À24.8 GX-22382 Forman and Ingolfsson! (2000) beach berm Whale ear bone from partially buried 6 93807140 À17.5 GX-22379 Forman and Ingolfsson! (2000) skull, collagen fraction Mya truncata shells from raised beach 6 9410760 À17.5 Salvigsen and Nydal (1981) Articulated Balanus balanus 10 9210760 +1.9 GX-22386 Forman and Ingolfsson! (2000) Storøya: marine limit 6671 m aht Driftwood 5.8 2965785 ST-7987 Jonsson (1983) Driftwood 7.6 3190785 ST-7986 Jonsson (1983) Driftwood 13.2 4075790 ST-7985 Jonsson (1983) Driftwood 20.0 5375795 ST-7827 Jonsson (1983) Driftwood 41.6 86857100 ST-7824 Jonsson (1983) Driftwood 44.0 86107120 ST-7984 Jonsson (1983) Driftwood 51.0 89357125 ST-7826 Jonsson (1983) Driftwood 53.3 92657125 ST-7825 Jonsson (1983)

1 The marine reservoir correction for shell, whalebone, walrus bone and seaweed is 440 years (Mangerud and Gulliksen (1975); Olsson (1980)). 2 These values for d13C are assumed.

Appendix B

Radiocarbon ages on driftwood and associated marine subfossils from raised beach sequences on Franz Josef Land, Russia (Table 3).

Table 3 The radiocarbon ages on driftwood and associated marine fossils on Franz Josef Land are presented in Table 3

Dated material Shoreline Laboratory 14C 13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Alexandra Land: marine limit 23.571 m aht Driftwood 5.0 1655770 St-12664 Glazovskiy et al. (1992) Driftwood 5 15507115 Mo-421 Grosswald (1973) Driftwood 8–9 3000755 Kovaleva et al. (1974) Driftwood 8.5 3385770 St-12668 Glazovskiy et al. (1992) Driftwood 10 4250790 Le-179 Dibner (1965) Driftwood 10 4520760 Kovaleva et al. (1974) Shells 15 7825790 St-12783 Glazovskiy et al. (1992) Driftwood 15.5 4980775 St-12665 Glazovskiy et al. (1992) Algae peat 17.5 55007235 Mo-355 Grosswald (1973) Driftwood >19.0 81307115 St-12782 Glazovskiy et al. (1992) Driftwood >14.0 8150750 Beta 58703 Naslund. et al. (1994) Whalebone >13.0 88507180 St-13901 Naslund. et al. (1994) Driftwood 18–20 4600750 Kovaleva et al. (1974) Driftwood 20–22 6760770 Kovaleva et al. (1974) Driftwood 21.5 6765775 St-12666 Glazovskiy et al. (1992) Driftwood 23.0 6090770 St-12663 Glazovskiy et al. (1992) ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1425

Table 3 (continued)

Dated material Shoreline Laboratory 14C 13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Bell Island: marine limit 4971 m aht 1.5-m long log on raised beach above 3 1050785 À25.6 GX-19476 Forman et al. (1996) storm limit 1.5-m long log embedded into raised 6 22057110 À24.6 GX-19570 Forman et al. (1996) beach Whale vertebrae on raised beach 9 2800785 À16.7 GX-19471G2 Forman et al. (1996) Whale skull fragment on buried in 13 3905790 À16.5 GX-19472G2 Forman et al. (1996) raised beach 3-m long whale jaw bone on raised 16 4255790 À16.7 GX-19473G2 Forman et al. (1996) spit Whale skull fragment on buried in 23 5465790 À16.9 GX-19474G2 Forman et al. (1996) raised beach Driftwood at marine escarpment 27 60457125 À22.2 GX-19475 Forman et al. (1996) Driftwood embedded into raised 45 97057105 À24.5 GX-17208 Forman et al. (1996) beach 2-m long whale ribimbeddedin 47 92207120 À17.1 GX-17209G2 Forman et al. (1996) raised beach Northbrook Island: marine limit 4371 m aht 1.5-m long whale ribimbeddedin 3 1425780 À16.6 GX-19483G2 Forman et al. (1996) raised beach Whale vertebrae disc imbedded in 8 24057105 À16.5 GX-19484G2 Forman et al. (1996) raised beach 2-m long log on raised beach 13 39507110 À24.3 GX-19485 Forman et al. (1996) 1.2-m long log on descending raised 18 4380790 À24.6 GX-19486 Forman et al. (1996) beach 1-m long log on raised beach 22 4435770 À25.0 AA-15679 Forman et al. (1996) 1-m long log on raised beach 30 6300765 À26.2 AA-16586 Forman et al. (1996) Whale vertebrae on raised beach 36 92207165 À18.0 GX-19487G2 Forman et al. (1996)

Southeastern George Island: marine limit 3871 m aht 0.5-m long log on raised beach above 4 1340780 À26.1 GX-19477 Forman et al. (1996) storm limit 2.5-m long log on raised beach 7 2180780 À25.3 GX-19478 Forman et al. (1996) 3-m long log in swale of raised beach 9 24807100 À23.2 GX-19479 Forman et al. (1996) 5-m long log on descending raised 15 3860790Ã À24.5 GX-19480 Forman et al. (1996) beach 1-m long tree root-plate fragment on 18 45657115 À24.5 GX-19481 Forman et al. (1996) raised beach 3-m long log on descending raised 20 4785795 À24.4 GX-19482 Forman et al. (1996) beach Paired Mya tnuncata from glacial >20 5035770 0 AA-12482 Forman et al. (1996) marine silt Hooker (H) and Scott Keltie (S) Islands: marine limit 3871 m aht 0.5-m long log on raised beach (H) 1 775755 À24.7 GX-17200 Forman et al. (1996) 0.5-m long log on raised beach (H) 2 1110780 À23.8 GX-17199 Forman et al. (1996) Driftwood on low raised beach (S) 5 22157125 À24.6 GX-17187 Forman et al. (1996) Driftwood on raised beach (S) 8 29707145 À23.0 GX-17188 Forman et al. (1996) 0.5-m long log wedged into raised 9 2655775 À26.2 AA-16587 Forman et al. (1996) beach (H) Driftwood on raised beach (S) 12 4485775 À25.0 GX-17191 Forman et al. (1996) Driftwood on raised beach (S) 16 4640775 À21.5 GX-17189 Forman et al. (1996) Whalebone embedded in beach berm 23.4 68407115 — GX-21246G2 Weihe (1996) (H) Whalebone at base of berm (H) 24.7 59407120 — GX-21244G2 Weihe (1996) Driftwood on raised beach (S) 26 6590785 À24.4 GX-17190 Forman et al. (1996) Whale vertebrae disc imbedded in 26 6555795 À17.4 GX-17558G2 Forman et al. (1996) raised beach (H) Driftwood 26 74457135 Mo-195 Grosswald (1973) 1.5-m long log on descending raised 29 72457100 À25.6 GX-17556 Forman et al. (1996) beach (H) ARTICLE IN PRESS 1426 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Table 3 (continued)

Dated material Shoreline Laboratory 14C 13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

1+m long log buried in raised beach 30 87157100 À25.0 GX-17198 Forman et al. (1996) (H) Driftwood on top of raised berm 30.6 77707140 — GX-21245 Weihe (1996) Whale vertebrae on raised beach (H) 32 75607295 À19.3 GX-17557G2 Forman et al. (1996) Whale vertebrae on raised beach (H) 33 94157125 À17.8 GX-17197G2 Forman et al. (1996) 96207230 À13.1 GX-17197A3 Forman et al. (1996) Whalebone (H) 35 95457175 — GX-21247G2 Weihe (1996) Paired Mya truncata from marine 30(36) 10,2907115 À0.3 GX-17266 Forman et al. (1996) sand (H) Paired Mya truncata from marine 32(36) 9995785 04 AA-8566 Forman et al. (1996) sand (H) Paired Mya truncata from marine 34(36) 9645780 04 AA-8567 Forman et al. (1996) sand (H) Driftwood 2-m below the marine 36 96707140 — GX-21249 Weihe (1996) limit (H) Mya truncata fragment from marine 37 9690790 — AA-19032 Weihe (1996) sand (H) Mya truncata fragment from marine 34 9890790 — AA-19033 Weihe (1996) sand (H) Driftwood just below the marine limit 37 99657145 — GX-21248 Weihe (1996) (S)

Cape Dandy, Hooker Island: marine limit 3871 m aht Driftwood from 2nd youngest non- 2.1 505755 AA-19697 Lubinski (1998) modern beach Driftwood from youngest non- 2.4 745755 AA-18995 Lubinski (1998) modern beach >1.5-m long driftwood log 3.6 1045750 AA-18997 Lubinski (1998) Driftwood partial buried by beach 3.0 1180750 AA-18996 Lubinski (1998) gravels >1.5-m long driftwood log partial 4.5 1635770 AA-19698 Lubinski (1998) buried in beach gravels Driftwood, root plate 6.6 2190760 AA-19699 Lubinski (1998) Driftwood mostly buried in beach 10.1 2480760 AA-18998 Lubinski (1998) gravels >1.5-m long driftwood log partial 11.1 3265770 AA-18999 Lubinski (1998) buried in beach gravels Driftwood, root plate 14.6 3750765 AA-19701 Lubinski (1998) Driftwood mostly buried in beach 14.0 3765765 AA-19700 Lubinski (1998) gravels 5-m long driftwood log partial buried 18.2 4445755 AA-19001 Lubinski (1998) in beach gravels Driftwood mostly buried in beach 19.0 4625755 AA-19000 Lubinski (1998) gravels Driftwood mostly buried in beach 21.0 5295780 AA-19002 Lubinski (1998) gravels >1.5-m long driftwood log 22.9 5645760 AA-19003 Lubinski (1998) 0.4-m long log mostly buried in beach 27.6 7010770 AA-19004 Lubinski (1998) gravels

Koettlitz (K) and Nansen (N) Islands: marine limit 2972 m aht Driftwood on raised beach (K) 5 1500760 À22.0 GX-17195 Forman et al. (1996) Driftwood on raised beach (K) 7 2410770 À24.7 GX-17194 Forman et al. (1996) Driftwood on raised beach (K) 10 29807125 À24.3 GX-17193 Forman et al. (1996) 1.5-m long log from raised beach (K) 16 4235775 GX-17192 Forman et al. (1996) Paired Mya truncata from sublittoral 26(29) 10,2907115 +1.1 GX-17267 Forman et al. (1996) sand (K) Paired Hiatella arctica from littoral 25(26) 6190760 04 AA-7902 Forman et al. (1996) gravel and sand (K) 0.5-m long log on raised beach (N) 27 10,3607115 À24.0 GX-17196 Forman et al. (1996) ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1427

Table 3 (continued)

Dated material Shoreline Laboratory 14C 13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Etheridge Island: highest raised beach 2871 m aht 2+m long log on descending raised 4 1075765 À25.3 GX-17559 Forman et al. (1997) beach 1.5-m long log behind berm of raised 16 4215780 À25.3 GX-17202 Forman et al. (1997) beach 1+m long log behind berm of raised 21 5000780 À22.8 GX-17203 Forman et al. (1997) beach 1-m long log on descending raised 23 4890780 À22.3 GX-17204 Forman et al. (1997) beach

Brady Island: marine limit 3471 m aht 2-m long log on raised beach 5 2560785 À23.8 GX-19489 Forman et al. (1997) 1-m long log on raised beach 9 39557110 À24.6 GX-19488 Forman et al. (1997) 2-m long tree root-plate buried in 12 4150790 À26.9 GX-19490 Forman et al. (1997) raised beach Whale skull partially buried in raised 16 4855780Ã À16.9 GX-20740G2 Forman et al. (1997) beach 0.5-m long tree root-plate buried in 19 5100795 À24.4 GX-19491 Forman et al. (1997) raised beach 1-m long log on raised beach 21 59807100 À24.5 GX-19492 Forman et al. (1997) 0.3-m long wood fragments within 29 81357115 À25.4 GX-19493 Forman et al. (1997) raised beach

Leigh Smith Island: marine limit 4072 m aht 3-m long log on raised beach 5 1055765 À26.0 GX-20741 Forman et al. (1997) 0.5-m long tree root-plate buried in 10 2010775 À23.6 GX-20742 Forman et al. (1997) raised beach 1-m long log in raised beach 14 2790770 À24.0 GX-20743 Forman et al. (1997) 8-m long log on raised beach 19 4555780 À25.1 GX-20744 Forman et al. (1997) 3-m long log buried in raised beach 25 5080780 À23.4 GX-20745 Forman et al. (1997)

Haves (H), Fersman (F) and Newcombe (N) islands: marine limit 2171 m aht 1.5-m long log buried in raised beach 1 1075760 À25.1 GX-18307 Forman et al. (1997) (H) 1.5-m long log on raised beach (N) 1.5 1830765 À25.8 GX-18316 Forman et al. (1997) 2-m long log on raised beach (N) 3 2040765 À27.6 GX-18312 Forman et al. (1997) 4+m long log on raised beach (F) 6 29807125 À24.7 GX-18310 Forman et al. (1997) 1-m long tree root-plate buried in 8 36357135 À26.3 GX-18309 Forman et al. (1997) raised beach (F) 1-m long tree root-plate buried in 9 38857140 À25.5 GX-18315 Forman et al. (1997) raised beach (N) Driftwood 10 47757115 Mo-239 Grosswald (1963) 3-m long log on raised beach (N) 12 4315775 À27.2 GX-18314 Forman et al. (1997) 2-m long whale ribimbeddedinto 17 4935780 À17.2 GX-18313G2 Forman et al. (1997) raised beach (N) 2-m long whale ribimbeddedinto 17 47757165 À15.3 GX-18313A3 Forman et al. (1997) raised beach (N) 0.5-m long log on raised beach (H) 17 5435780 À25.0 GX-18308 Forman et al. (1997) Paired Mya truncata from marine >5 5090765Ã 04 AA-10247 Forman et al. (1997) muds (H) Driftwood (H) 10 47757115 Grosswald (1963)

Champ (C) and Wiener Neustadt (W) islands Mya truncata valve from sublittoral >9 9386790Ã +0.7 GX-19027- Forman et al. (1997) sand (C) AMS Hiatella arctica valve from sublittoral >3 89707100 +0.9 GX-21170- Forman et al. (1997) sand (W) AMS

Klagenfurt Island: Marine Limit 2071 m aht 1-m long log on raised beach 4 1850765 À23.8 GX-18298 Forman et al. (1997) 1.5-m long log on raised beach 7 3195770 À25.2 GX-18297 Forman et al. (1997) ARTICLE IN PRESS 1428 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Table 3 (continued)

Dated material Shoreline Laboratory 14C 13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

1-m long tree root-plate buried in 10 3635775 À24.6 GX-18294 Forman et al. (1997) raised beach 0.5-m long tree root-plate buried in 14 48707155 À25.4 GX-18295 Forman et al. (1997) raised beach 0.75-m long log on raised beach 16 48307115 À24.6 GX-2136 Forman et al. (1997) 1-m long log on raised beach 17 49257160 À26.4 GX-18296 Forman et al. (1997)

Wilczek Island: Marine Limit 2571 m aht 0.75-m long log buried in raised beach 4 9757105 À24.6 GX-18299 Forman et al. (1997) 2-m long log on raised beach 6 20407115 À26.3 GX-18300 Forman et al. (1997) 2.5-m long log on raised beach 10 32957130 À25.2 GX-18301 Forman et al. (1997) 0.75-m long log buried in raised beach 12 36607100 À26.1 GX-21367 Forman et al. (1997) 1-m long log on raised beach 15 5255780 À25.7 GX-18302 Forman et al. (1997) Fragment from whale skull 16 44257110Ã À17.0 GX-21366G2 Forman et al. (1997) 1.5-m long log on raised beach 18 5205780 À24.6 GX-18303 Forman et al. (1997) 1.5-m long log on raised beach 20 5830785 À26.9 GX-18304 Forman et al. (1997) Walrus skull in raised beach 22 5880785Ã À16.5 GX-18306G2 Forman et al. (1997) 50307170Ã À11.6 GX-18306A3 Forman et al. (1997)

Koldewey Island: marine limit 2471 m aht 2-m long log in raised beach behind 2 1100770 À25.0 GX-19507 Forman et al. (1997) storm beach 1.5-m long log on raised beach 3 14657105 À22.9 GX-19501 Forman et al. (1997) 0.75-m long log on raised beach 14 1645770 À26.0 GX-20748 Forman et al. (1997) 2 m-long log on raised beach 6 28707105 À26.8 GX-19502 Forman et al. (1997) 1.5-m long log on raised beach 16 3230785 À27.1 GX-19504 Forman et al. (1997) 1-m long in raised beach 10 3625790 À26.1 GX-19503 Forman et al. (1997) 2-m long log in raised beach 20 6055795 À25.9 GX-20747 Forman et al. (1997) 0.5-m long tree root-plate buried in 21 64707100 À24.8 GX-19505 Forman et al. (1997) raised beach 0.5-m long log on raised beach 23 73357105 À25.3 GX-19506 Forman et al. (1997) 5-m long log in raised beach at marine 24 79807140 À25.8 GX-19508 Forman et al. (1997) limit

Outer Hall Island: marine limit 3272 m aht 1-m long log in raised beach 4 13257105 À23.7 GX-19496 Forman et al. (1997) 1-m long log in raised beach 7 2265785 À24.6 GX-19497 Forman et al. (1997) 0.75-m long tree root-plate buried in 9 3515785 À23.4 GX-19498 Forman et al. (1997) raised beach 1-m long log on raised beach 11 3770790 À25.1 GX-19515 Forman et al. (1997) 0.3-m long wood fragments within 18 5010795 À25.7 GX-19500 Forman et al. (1997) raised beach 1.5-long log buried in raised beach 23 64907130 À25.2 GX-19494 Forman et al. (1997) 1-m long log buried in raised beach 31 86557145 À24.4 GX-19495 Forman et al. (1997)

Severe Bay, Hall Island: marine limit 2372 m aht 2-m long splinter log found on raised 23 83107145 À24.6 GX-19512 Forman et al. (1997) beach Whale skull from washed sublittoral >8 94507165 17.3 GX-19511G2 Forman et al. (1997) sediments Paired valves of Mya truncata from >3 96557100Ã +1.9 GX-19509 Forman et al. (1997) delatic sands Paired valves of Mya truncata from >7 82607115Ã +0.9 GX-19510 Forman et al. (1997) delatic sands

1 440 years has been subtracted from 14C ages on marine subfossils to compensate for the 14C oceanic reservoir effect (Mangerud and Gulliksen (1975); Olsson (1980); Forman and Polyak (1997)). 2 The collagen-dominated gelatin extract for all whalebones was dated. 3 Radiocarbon age on the apatite extract. 4 A 13C value of 0 was assumed for marine carbonate analyzed by the National AMS facility at the University of Arizona. ARTICLE IN PRESS S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434 1429

Appendix C

Radiocarbon ages on driftwood and associated marine subfossils from raised beach sequences Novaya Zemlya and Vaygach Island, Russia (Table 4).

Table 4 The radiocarbon ages on driftwood and associated marine subfossils from Novaya Zemlya and Vaygach Island, Russia is presented in Table 4

Dated material Shoreline Laboratory 14C 13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Cape Bismarck: marine limit 1371 m aht Partially buried 1.5-m long log 12.5 (10) 5365760 À24.7 GX-25466 Zeeberg et al. (2001) Whale vertebra 10 3710775 À16.8 GX-25467G Zeeberg et al. (2001) Driftwood log 2.5 m long 10 3485785 À25.1 GX-24850 Zeeberg et al. (2001) Decayed 2-m long log 7.2 2985750 À24.2 GX-24851 Zeeberg et al. (2001) Root section 6.7 1365740 À25.5 GX-25465 Zeeberg et al. (2001) Decayed 7-m long log 5.1 1350750 À25.6 GX-24852 Zeeberg et al. (2001) Partially buried 8-m long log 4.7 1875750 À26.2 GX-24853 Zeeberg et al. (2001)

Cape Spory Navolok: marine limit o13 m aht Log partially buried 12 48607140 À26.4 GX-18532 Zeeberg et al. (2001) 3-m long log partially buried 4.5 2955780 À25.4 GX-23233 Zeeberg et al. (2001) Willem Barents’ ship timber 2 360 Gawronski and Zeeberg (1997)

Cape Zhelaniya: marine limit >10.5 m aht Root section 1.5-m 7.1 4380760 À25.8 GX-25459 Zeeberg et al. (2001) Log 5-m long from snow bank 6.5 4000785 À24.6 GX-24835 Zeeberg et al. (2001) Log 2-m long from solifluction 6.1 3710780 À26.3 GX-24837 Zeeberg et al. (2001) Log >l-m long partially buried 4.2 3200780 À23.8 GX-24838 Zeeberg et al. (2001) Log 5-m long partially buried 3.8 3205755 À24.7 GX-24839 Zeeberg et al. (2001) Log >1 m long partially buried 3.7 1930745 À25.1 GX-25460 Zeeberg et al. (2001) Log 2.5-m long partially buried 3.5 1570770 À26.8 GX-24840 Zeeberg et al. (2001) Log 5-m long partially buried 1.9 795765 À23.9 GX-24841 Zeeberg et al. (2001) Log 5-m long partially buried 1.4 770765 À25.7 GX-24842 Zeeberg et al. (2001)

Ivanov Bay: marine limit 13.571 m aht Whalebone 13.5 (12) 68857105 À17.2 GX-24843G2 Zeeberg et al. (2001) Whalebone 13.5 (12) 70807105 À17.1 GX-24844G2 Zeeberg et al. (2001) Partially buried 3-m long log 8.8 3760745 À23.8 GX-25464 Zeeberg et al. (2001) Partially buried 3-m long log 7.8 3530750 À24.5 GX-24845 Zeeberg et al. (2001) Partially buried 2-m long log 6.8 2805750 À25.3 GX-24846 Zeeberg et al. (2001) Partially buried 4-m long log 5 805755 À26.6 GX-24847 Zeeberg et al. (2001) Partially buried 2.5-m long log 4.3 575740 À23.0 GX-25462 Zeeberg et al. (2001) Partially buried >5-m long log 4.2 1830750 À26.4 GX-24848 Zeeberg et al. (2001)

Cape Medvezhy: marine limit 1271 m aht Log 3-m long from base of solifluction lobe 10.5(10) 4070755 À26.1 GX-24864 Zeeberg et al. (2001) Log o2.5-m long from snow bank 9 3635750 À25.9 GX-24863 Zeeberg et al. (2001) Partially buried >3-m long log 6.9 3070750 À25.8 GX-24860 Zeeberg et al. (2001) Decayed, part buried 7-m long log 6.2 2125775 À26.1 GX-24861 Zeeberg et al. (2001) Partially buried 2.5-m long log 5.6 1665750 À24.8 GX-24862 Zeeberg et al. (2001) Decayed, part buried 4-m long log 4.4 945755 À26.6 GX-24859 Zeeberg et al. (2001) Decayed, part buried 2.2-m long log 3.8 295750 À27.3 GX-24858 Zeeberg et al. (2001)

Russkaya Gavan’: marine limit 1271 m aht Partially buried B2-m long log 6.5 4145750 À25.3 GX-24857 Zeeberg et al. (2001) Buried B3-m long log 3.6 2890750 À24.3 GX-25469 Zeeberg et al. (2001) Log 3-m long 3.6 3105775 À23.6 GX-24856 Zeeberg et al. (2001) Partially buried B3-m long log 2.9 1535750 À25.2 GX-24855 Zeeberg et al. (2001) Root of 4-m long log 2.1 600745 À24.4 GX-25468 Zeeberg et al. (2001) Decayed 7-m long log 1.9 175775 À25.7 GX-24854 Zeeberg et al. (2001) ARTICLE IN PRESS 1430 S.L. Forman et al. / Quaternary Science Reviews 23 (2004) 1391–1434

Table 4 (continued)

Dated material Shoreline Laboratory 14C 13C Laboratory Reference altitude age or reservoir number (m aht) corrected age1 (yr BP)

Nordenskiold. Bay: marine limit 1171 m aht 1.5-m log on vegetated surface above storm 2 445760 À24.8 GX-17899 Forman et al. (1999a,b) beach Wave abraded 1-m long log in beach gravels 3.5 1380765 À25.6 GX-18318 Forman et al. (1999a,b) Whale vertebrae buried in beach gravels 5 17257120 À23.5 GX-18317G2 Forman et al. (1999a,b) 20407120 À11.3 GX-18317A3 Forman et al. (1999a,b) 1.5-m long log behind raised beach berm 5.5 1510765 À23.5 GX-17898 Forman et al. (1999a,b) Walrus jaw bone on raised beach 8 3775775 À14.6 GX-18320G2 Forman et al. (1999a,b) 26657130 À9.2 GX-18320A3 Forman et al. (1999a,b) Whalebone partially buried in beach gravels 9 3625775 À17.0 GX-18319G2 Forman et al. (1999a,b) 37507170 À13.9 GX-18319A3 Forman et al. (1999a,b)

Vilkitskiy Bay: marine limit 1071 m aht 5-m log on partially buried in beach gravels 3 8057105 À24.8 GX-18290 Forman et al. (1999a,b) Whale vertebrae buried in beach gravels 8 4425780 À16.8 GX-18291G2 Forman et al. (1999a,b) 43257145 À14.5 GX-18291A3 Forman et al. (1999a,b)

Vise Glacier-Inostrantsev Bay: marine limit 1071 m aht 1-m log on partially buried in beach gravels 3 7907105 À25.3 GX-18292 Forman et al. (1999a,b) 3-m log on buried in beach gravels 5 24707120 À26.1 GX-18293 Forman et al. (1999a,b)

Vaygach Island: Cape Bolvansky, marine limit B2 m aht Partially buried 2.5-m long log 1.6 540750 À25.6 GX-27227 Zeeberg et al. (2001) Partially buried B2-m long log 1 470740 À25.5 GX-27229 Zeeberg et al. (2001) Partially buried root section of log o1 270740 À24.9 GX-27228 Zeeberg et al. (2001) 1 440 years has been subtracted from 14C ages on marine subfossils to compensate for the 14C oceanic reservoir effect (Mangerud and Gulliksen (1975); Olsson (1980); Forman and Polyak (1997)). 2 The collagen-dominated gelatin extract for all whalebones was dated. 3 Radiocarbon age on the apatite extract.

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