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href="https://ntnu-no.academia.edu/James_H_Barrett">James H Barrett</a><p class="suggested-user-card__user-info__subheader ds2-5-body-xs">Norwegian University of Science and Technology</p></div></div><div class="suggested-user-card"><div class="suggested-user-card__avatar social-profile-avatar-container"><a data-nosnippet="" href="https://uio.academia.edu/VivianWangen"><img class="profile-avatar u-positionAbsolute" alt="Vivian Wangen related author profile picture" border="0" src="//a.academia-assets.com/images/s200_no_pic.png" /></a></div><div class="suggested-user-card__user-info"><a class="suggested-user-card__user-info__header ds2-5-body-sm-bold ds2-5-body-link" href="https://uio.academia.edu/VivianWangen">Vivian Wangen</a><p class="suggested-user-card__user-info__subheader ds2-5-body-xs">University of Oslo</p></div></div><div class="suggested-user-card"><div class="suggested-user-card__avatar social-profile-avatar-container"><a data-nosnippet="" 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title="Journal Articles"><span>1</span> <span class="ds2-5-body-sm-bold">Journal Articles</span></a></li></ul></div><div class="divider ds-divider-16" style="margin: 0px;"></div><div class="documents-container backbone-social-profile-documents" style="width: 100%;"><div class="u-taCenter"></div><div class="profile--tab_content_container js-tab-pane tab-pane active" id="all"><div class="profile--tab_heading_container js-section-heading" data-section="Papers" id="Papers"><h3 class="profile--tab_heading_container">Papers by Atle Nesje</h3></div><div class="js-work-strip profile--work_container" data-work-id="1360476"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/1360476/Holocene_glaciation_and_climate_evolution_of_Baffin_Island_Arctic_Canada"><img alt="Research paper thumbnail of Holocene glaciation and climate evolution of Baffin Island, Arctic Canada" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Holocene glaciation and climate evolution of Baffin Island, Arctic Canada</div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://uib.academia.edu/AtleNesje">Atle Nesje</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://indiana.academia.edu/PeterSauer">Peter E Sauer</a></span></div><div class="wp-workCard_item"><span>Quaternary Science …</span><span>, Jan 1, 2005</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Lake sediment cores and cosmogenic exposure (CE) dates constrain the pattern of deglaciation and ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Lake sediment cores and cosmogenic exposure (CE) dates constrain the pattern of deglaciation and evolution of climate across Baffin Island since the last glacial maximum (LGM). CE dating of erratics demonstrates that the northeastern coastal lowlands became ice-free ca.14ka as the Laurentide Ice Sheet (LIS) receded from its LGM margin on the continental shelf. Coastal lakes in southeastern Baffin Island</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="1360476"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="1360476"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 1360476; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=1360476]").text(description); $(".js-view-count[data-work-id=1360476]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 1360476; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='1360476']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=1360476]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":1360476,"title":"Holocene glaciation and climate evolution of Baffin Island, Arctic Canada","translated_title":"","metadata":{"abstract":"Lake sediment cores and cosmogenic exposure (CE) dates constrain the pattern of deglaciation and evolution of climate across Baffin Island since the last glacial maximum (LGM). 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-1360476-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874042"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874042/Geometry_thickness_and_isostatic_loading_of_the_late_weichselian_scandinavian_ice_sheet"><img alt="Research paper thumbnail of Geometry, thickness and isostatic loading of the late weichselian scandinavian ice sheet" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Geometry, thickness and isostatic loading of the late weichselian scandinavian ice sheet</div><div class="wp-workCard_item"><span>Norsk Geologisk Tidsskrift</span><span>, 1992</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874042"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874042"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874042; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874042-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874041"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874041/Quantification_of_late_Cenozoic_erosion_and_denudation_in_the_Sognefjord_drainage_basin_western_Norway"><img alt="Research paper thumbnail of Quantification of late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Quantification of late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway</div><div class="wp-workCard_item"><span>Norsk Geogr Tidsskr Nor J Geo</span><span>, 1994</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT The total late Cenozoic erosion and denudation in the Sognefjord drainage basin, western...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT The total late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway, has been calculated to about 5400 km3 by subtracting the present topography from a reconstructed preglacial (paléic) surface. This volume corresponds to a mean erosion and denudation of 440 m in the Sognefjord drainage basin. The total volume of subaerial denudation and fluvial activity amounts to about 400 km3. The remaining volume of about 5000 km3 yields a mean glacial erosion of about 400 m in the Sognefjord drainage basin. Assuming glacial erosion in a period of 1 million years during the past 2.57 million years, the average rate of glacial erosion in the Sognefjord drainage basin was about 40cm 1000 yr-1 (0.4mm yr-1).</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874041"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874041"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874041; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874041]").text(description); $(".js-view-count[data-work-id=30874041]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874041; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874041']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=30874041]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874041,"title":"Quantification of late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway","translated_title":"","metadata":{"abstract":"ABSTRACT The total late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway, has been calculated to about 5400 km3 by subtracting the present topography from a reconstructed preglacial (paléic) surface. This volume corresponds to a mean erosion and denudation of 440 m in the Sognefjord drainage basin. The total volume of subaerial denudation and fluvial activity amounts to about 400 km3. The remaining volume of about 5000 km3 yields a mean glacial erosion of about 400 m in the Sognefjord drainage basin. Assuming glacial erosion in a period of 1 million years during the past 2.57 million years, the average rate of glacial erosion in the Sognefjord drainage basin was about 40cm 1000 yr-1 (0.4mm yr-1).","publication_date":{"day":null,"month":null,"year":1994,"errors":{}},"publication_name":"Norsk Geogr Tidsskr Nor J Geo"},"translated_abstract":"ABSTRACT The total late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway, has been calculated to about 5400 km3 by subtracting the present topography from a reconstructed preglacial (paléic) surface. This volume corresponds to a mean erosion and denudation of 440 m in the Sognefjord drainage basin. The total volume of subaerial denudation and fluvial activity amounts to about 400 km3. The remaining volume of about 5000 km3 yields a mean glacial erosion of about 400 m in the Sognefjord drainage basin. Assuming glacial erosion in a period of 1 million years during the past 2.57 million years, the average rate of glacial erosion in the Sognefjord drainage basin was about 40cm 1000 yr-1 (0.4mm yr-1).","internal_url":"https://www.academia.edu/30874041/Quantification_of_late_Cenozoic_erosion_and_denudation_in_the_Sognefjord_drainage_basin_western_Norway","translated_internal_url":"","created_at":"2017-01-11T05:01:33.864-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Quantification_of_late_Cenozoic_erosion_and_denudation_in_the_Sognefjord_drainage_basin_western_Norway","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"ABSTRACT The total late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway, has been calculated to about 5400 km3 by subtracting the present topography from a reconstructed preglacial (paléic) surface. This volume corresponds to a mean erosion and denudation of 440 m in the Sognefjord drainage basin. The total volume of subaerial denudation and fluvial activity amounts to about 400 km3. The remaining volume of about 5000 km3 yields a mean glacial erosion of about 400 m in the Sognefjord drainage basin. Assuming glacial erosion in a period of 1 million years during the past 2.57 million years, the average rate of glacial erosion in the Sognefjord drainage basin was about 40cm 1000 yr-1 (0.4mm yr-1).","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[],"research_interests":[{"id":262,"name":"Human Geography","url":"https://www.academia.edu/Documents/in/Human_Geography"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874041-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874040"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/30874040/Glacial_landforms_and_Quaternary_landscape_development_in_Norway"><img alt="Research paper thumbnail of Glacial landforms and Quaternary landscape development in Norway" class="work-thumbnail" src="https://attachments.academia-assets.com/51300480/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/30874040/Glacial_landforms_and_Quaternary_landscape_development_in_Norway">Glacial landforms and Quaternary landscape development in Norway</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The Norwegian landscape is a function of geological processes working over very long time spans, ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The Norwegian landscape is a function of geological processes working over very long time spans, and first order structures might for example be traced to the ancient denudational processes, the Caledonian orogeny or break-up of the North Atlantic. However, a large portion of large-, intermediate-, and small-scale landforms in Norway owe their existence to Quaternary glaciations or periglacial processes. The Quaternary time period (the last c. 3 million years), is characterised by cool and variable climate with temperatures oscillating between relative mildness to frigid ice-age conditions. A wide spectrum of climate-driven geomorphological processes has thus been acting in Norway, but the numerous glaciations have had the most profound effect with the production of large U-shaped valleys, fjords and Alpine relief. On the other hand, interior and upland areas in Norway seem to be largely unaffected by glacial erosion and exhibit a possibly pre-Quaternary landscape with only some periglacial influence. The ice sheets in Scandinavia thus have redistributed rock mass and sediments in the landscape with the largest glaciogenic deposits being found on the continental shelf. Large Quaternary deposits and valley fills can also be found onshore and these are now valuable resources for aggregates, ground water and agriculture. Important Quaternary processes have also been acting along the Norwegian coast with denudation of the famous strandflat, where the formation processes are not fully understood. The isostatic depression of crust under the vast ice sheets have also lead to important consequences, with thick deposits of potentially unstable, fine-grained glaciomarine sediments in quite large areas of Norway. It is thus clear that much of Norway's beauty but also geohazard problems can be explained with the actions of Quaternary geomorphological processes.</span></div><div class="wp-workCard_item"><div class="carousel-container carousel-container--sm" id="profile-work-30874040-figures"><div class="prev-slide-container js-prev-button-container"><button aria-label="Previous" class="carousel-navigation-button js-profile-work-30874040-figures-prev"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_back_ios</span></button></div><div class="slides-container js-slides-container"><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375406/figure-1-first-order-glacial-erosion-landforms-are-centred"><img alt="Figure 1. First-order glacial erosion landforms are centred around the Scandinavian mountain chain with fords on the Norwegian coast and deep piedmont lakes east of the mountains " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375407/figure-2-relict-nonglacial-surfaces-east-of-the-lyngen-fjord"><img alt="Figure 2. Relict nonglacial surfaces east of the Lyngen fjord in Troms. Note that all mountains reach essentially the same altitude and the very flat appearance of the surfaces. These surfaces have probably been connected into a flat, undulating landscape which was uplifted and eroded through fluvial and glacial processes in the Neogene. Total relief in the area, including the ford, is on the order of 2 km. It is evident that glacial erosion has altered the preglacial landscape profoundly in many areas but conversely it also seems likely that pre-Quaternary topography has conditioned glacial erosion. Pre-Quaternary fluvial valleys probably focused glacier ice flow early on in the Quaternary glacial history, thus creating a positive feedback where subsequent ice flow continued to deepen these valleys. It follows, which a large body of geomorphological literature also shows, that Quaternary glaciations have eroded the landscape selectively (e.g., Sugden 1978, Nesje and Whillans 1994, Lidmar-Bergstrém et al. 2000, Li et al. 2005, Fjellanger et al. 2006, Staiger et al. 2005, Phillips et al. 2006), creating mountainous areas with deeply incised troughs and virtually nonaffected uplands. These noneroded uplands are henceforth called relict nonglacial " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_002.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375408/figure-3-was-able-to-create-features-similar-to-both"><img alt="was able to create features similar to both crescentic fractures and gouges. Up-ice concave and convex features were shown to be conditioned by the effective pressure applied by the ball bearing during these experiments, where up-ice concave features preferably formed when a high level of pressure was applied (Smith 1984). Good examples of striae, crescentic fractures and gouges can e.g., be found in the coastal landscape of southern Norway and in front of contemporary glaciers. Roches moutonées and rock drumlins are bedrock cnolls that have been polished by glacial abrasion. Depending yn bedrock joints and grains these landforms often become he glacier has evacuated pre-Quaternary) topogra ‘longated in the ice-flow direction and are thus excellent ndicators of former ice flow. Roches moutonées differ from ‘ock drumlins in that they have a plucked lee-side slope, where parts of the bedrock knoll, probably hrough freeze-on processes. It is debated whether roches noutonées and rock drumlins are governed by a pre-existing phy, perhaps akin to a stripped etch urface or if they are primarily formed by glacial abrasion Lindstr6m 1988, Johansson et al. 2001). Many areas in outhern Norway exhibit beautiful Roches moutonées and rock rumlins; this is probably due to rapid ice movement in the ‘un-up zone for the Norwegian channel ice stream (Sejrup et U. 2000, 2003). knolls that have been polished by glacial abrasion. Depending " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_003.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375409/figure-4-shaped-valley-with-overdeepened-lake-basin-at-lake"><img alt="Figure 4, U-shaped valley with overdeepened lake basin at lake Loen close to Nordford, western Norway Fjords are essentially glacial troughs cut into bedrock below today’s sea level and is perhaps the most prominent landscape feature in Norway (Figure 4). Fjords are formed much in the same way as U-shaped valleys although the overdeepening in fjords may be even more pronounced forming sills at the fford mouth (Lysa et al. 2009). It is thought that these sills were formed due to less glacial erosion at the coast where the former ice tongues spread out and became thinner (Aarseth 1997). As with U-shaped valleys, fords often follows fault zones, which may give rise to distinct fjord networks as is evident for example on the Mare coast (Gabrielsen et al. 2002). Fjords are important sinks for interglacial sediments (Aarseth 1997, Lysa et al. 2009). Indeed Aarseth (1997), calculated that about 150 km3 Holocene sediments reside in the main Norwegian fjords. Aarseth (1997) also considered most fjord sediments to be evacuated during main glaciations and, consequently, transported and deposited onto the continental shelf or shelf break. Subglacial channels may be formed by highly pressurised water, which is governed by the hydraulic potential gradient within the glacier. The subglacial water may thus defy gravity and cause subglacial meltwater channels that are at odds with topography or with an irregular longitudinal profile. Subglacial meltwater channels, naturally, require flowing water beneath the ice and thus indicate warm-based ice. Subglacial channels may be formed by highly pressurised " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_004.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375411/figure-6-smaller-glaciofluvial-erosional-landforms-include"><img alt="Smaller glaciofluvial erosional landforms include potholes (Figure 6) and P-forms. These are local features that are thought to represent highly dynamical, subglacial conditions where large volumes of meltwater are involved (Dahl 1965). formed through the catastrophic drainage of the vast “Nedre Glamsjo’ ice dammed lake about 10,300 years ago (Longva and Toresen 1991). " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_005.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375413/figure-7-end-moraines-or-more-generally-ice-marginal"><img alt="End moraines or more generally ice-marginal moraines are formed at the glacier margin by either: 1) glacier dumping of debris, 2) ablation or freeze-out of debris and, 3) glaciotectonic processes including pushing of proglacial sediments. Other pro- cesses might also be involved, such as rockfall or slope processes depositing material at the glacier margin. A vast amount of lit- erature describes the various types of ice-marginal moraines and depositional processes (e.g., Clayton and Moran 1974, Boulton and Eyles 1979, Hambrey and Huddart 1995, Bennet 2001). End moraines are important glacial landforms since they in- dicate a glacier advance or still-stand and are thus diagnostic in reconstructing ice-sheet dynamics and configurations. One orwegian end moraine, the Vassryggen Younger Dryas end moraine southeast of Stavanger, was used by Jens Esmark to support the theory of ice ages already in 1824 (Worsley 2006, Figure 7). Ice-marginal moraines are common in Norway and are commonly found in the proglacial areas of present glaciers. Many of these end moraines were formed during the ‘Little Ice Age’ (maximum at about AD 1750) and subsequent glacier re- treat (Nesje et al. 1991, Mathews 2005, Burki et al. 2009). Also other Holocene end-moraine zones are common (e.g., Nesje and Kvamme 1991, Figure 8) but the most prominent ice-marginal " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_006.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375414/figure-8-the-olfjellet-moraine-in-nordland-of-likely-pre"><img alt="Figure 8. The Olfjellet moraine in Nordland of likely Pre-Boreal age. Note multiple and complex ridges indicating an oscillating ice margin " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_007.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375416/figure-9-rogen-moraine-at-hartkjolen-in-nord-trondelag"><img alt="Figure 9. Rogen moraine at Hartkjolen in Nord-Trondelag. " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_008.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375418/figure-10-drumlins-on-lista-in-south-norway-shown-in-shaded"><img alt="Figure 10. Drumlins on Lista in South Norway shown in a shaded relief map produced through high-resolution LiDAR digital-elevation data. The drumlins show ice flow from ENE towards the Skagerrak ice stream. " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_009.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375420/figure-10-terrain-such-as-in-jotunheimen-al-hattestrand"><img alt="terrain such as in Jotunheimen. al. 1989, Hattestrand 1997). Based on extensive mapping o ribbed moraines Kleman and Hattestrand (1999) argued that ribbed moraine forms at the transition between cold-based ice and warm-based ice, which is also indicated by Sollid and Sorbe (1994). Ribbed moraine might thus be a good indication of areas beneath an ice sheet where basal temperatures have been low. Extensive areas of ribbed moraine may be found in north- ernmost and eastern Norway (Sollid and Torp 1984, Sollid and Serbel 1994) and many smaller areas can be found in elevated terrain such as in Jotunheimen. " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_010.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375422/figure-11-glacial-striae-reported-by-vorren-and-sollid-and"><img alt="Glacial striae reported by Vorren (1977, 1979) and Sollid and Torp (1984) in South Norway are perhaps the only likely Landforms from the Early and Middle Weichselian (marine isotope stages 5—3) are rare, although several localities from many parts of Norway with Early to Middle Weichselian sediments have been reported (overviews by Mangerud 2004, Mangerud et al. 2011, Olsen et al. this volume). Much of the landform record from these stages has probably been obliterated in Norway by subsequent glacial stages, although widespread glacial-landform systems of Early Weichselian age have been reported from Sweden and Finland (e.g., Lagerback 1998, Hirvas 1991, Kleman 1992, Hattestrand 1998, Fredin and Hattestrand 2002). " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_011.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375424/figure-12-in-interior-areas-in-southeast-norway-there-are"><img alt="In interior areas in southeast Norway there are numerous sets of end moraines, drumlins, Rogen moraine and glacial meltwater channels that likely predate the last glacial maximum (Sollid and Sorbel 1994, Fredin 2004). Nice examples of supposedly pre-LGM meltwater channels and marginal moraines are for example found on and around the Stwlen mountains close to lake Femunden. This general supposition is based on the observation that these landforms are generally incompatible with known LGM and deglaciation ice-flow patterns in the area and considerations of the thermal regime in the ice (Sollid and Sorbel 1994, Fredin 2004). " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_012.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375426/figure-14-shaded-relief-in-combined-bathymetric-and"><img alt="Figure 14. Shaded relief in a combined bathymetric and topographic dataset show- ing the floor of Tafjord. Note the very large submarine rock-avalanche deposits in the fjord. 11). Because the main ice divide in South Norway was situated south of the water divide, large ice-dammed lakes formed, at least partly subglacially—sublaterally, during the deglaciation leading to deposition of ice-dammed lake deposits. When these lakes drained, extensive meltwater erosional landforms were formed together with erosional marks from floating icebergs (Longva and Thoresen 1991). to deposition of ice-dammed lake deposits. When these lakes " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_013.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375428/figure-18-shorelines-are-usually-erosional-landforms"><img alt="Shorelines are usually erosional landforms indicating wave action for a prolonged time period, and are thus indicative of a sustained sea-level stand. On the Norwegian coast, shorelines are common and the most pronounced shorelines typically reflect the highest sea-level stand following the deglaciation, the Younger Dryas ‘main line’, or the Tapes transgression shoreline at around 6300 BP (cf., Andersen 1968, Svendsen and Mangerud 1987, Sorensen et al. 1987, Reite et al. 1999, Romundset et al. 2011). Shorelines may also be formed at the shores of glacial lakes and perched shorelines may be found in abandoned glacial-lake basins. Somewhat related to shorelines are coastal caves, which are also created by coastal erosion (Figure 18). They typically form where a lithological weakness zone in coastal cliffs coincides in altitude with a prolonged sea-level stand, thus allowing wave erosion to act on the weakness zone. Coastal caves are found, e.g., on the More coast and probably date to the Eemian high sea-level stand (Larsen and Mangerud 1989). " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_014.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375430/figure-16-landscape-at-ulset-dominated-by-glaciomarine-clays"><img alt="Figure 16. A landscape at Ulset dominated by glaciomarine clays with significant quick-clay slide scars. " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_015.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375432/figure-16-the-strandflat-is-flat-bedrock-platform-along-most"><img alt="The strandflat is a flat bedrock platform along most of the Norwegian west coast, which extends both above and below Norwegian west coast, which extends both above and below " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_016.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375434/figure-17-gravitational-processes-by-structural-geology"><img alt="Gravitational processes by structural geology (bedrock competence and structure) and the " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_017.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375436/figure-20-photograph-of-potential-rock-avalanche-on"><img alt="Figure 20. Photograph of a potential rock avalanche on Nornesfellet, threatening to fall into the Lyngen fjord and thus jeopardising several communities in the area. There are several similar sites in the area. All are situated on relatively steep glacial trough walls in a zone of high seismic activity (Iain Henderson, pers. comm.). " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_018.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375438/figure-19-glacial-landforms-and-quaternary-landscape"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_019.jpg" /></a></figure></div><div class="next-slide-container js-next-button-container"><button aria-label="Next" class="carousel-navigation-button js-profile-work-30874040-figures-next"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_forward_ios</span></button></div></div></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="3eedc86c7b187333bbaad19f09f428ee" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":51300480,"asset_id":30874040,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/51300480/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874040"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874040"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874040; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874040]").text(description); $(".js-view-count[data-work-id=30874040]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874040; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874040']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "3eedc86c7b187333bbaad19f09f428ee" } } $('.js-work-strip[data-work-id=30874040]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874040,"title":"Glacial landforms and Quaternary landscape development in Norway","translated_title":"","metadata":{"ai_title_tag":"Quaternary Glacial Processes Shaping Norway's Landscape","grobid_abstract":"The Norwegian landscape is a function of geological processes working over very long time spans, and first order structures might for example be traced to the ancient denudational processes, the Caledonian orogeny or break-up of the North Atlantic. However, a large portion of large-, intermediate-, and small-scale landforms in Norway owe their existence to Quaternary glaciations or periglacial processes. The Quaternary time period (the last c. 3 million years), is characterised by cool and variable climate with temperatures oscillating between relative mildness to frigid ice-age conditions. A wide spectrum of climate-driven geomorphological processes has thus been acting in Norway, but the numerous glaciations have had the most profound effect with the production of large U-shaped valleys, fjords and Alpine relief. On the other hand, interior and upland areas in Norway seem to be largely unaffected by glacial erosion and exhibit a possibly pre-Quaternary landscape with only some periglacial influence. The ice sheets in Scandinavia thus have redistributed rock mass and sediments in the landscape with the largest glaciogenic deposits being found on the continental shelf. Large Quaternary deposits and valley fills can also be found onshore and these are now valuable resources for aggregates, ground water and agriculture. Important Quaternary processes have also been acting along the Norwegian coast with denudation of the famous strandflat, where the formation processes are not fully understood. The isostatic depression of crust under the vast ice sheets have also lead to important consequences, with thick deposits of potentially unstable, fine-grained glaciomarine sediments in quite large areas of Norway. It is thus clear that much of Norway's beauty but also geohazard problems can be explained with the actions of Quaternary geomorphological processes.","publication_date":{"day":1,"month":6,"year":2013,"errors":{}},"grobid_abstract_attachment_id":51300480},"translated_abstract":null,"internal_url":"https://www.academia.edu/30874040/Glacial_landforms_and_Quaternary_landscape_development_in_Norway","translated_internal_url":"","created_at":"2017-01-11T05:01:33.459-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":51300480,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300480/thumbnails/1.jpg","file_name":"Glacial_landforms_and_Quaternary_landsca20170111-6810-1gmlzqp.pdf","download_url":"https://www.academia.edu/attachments/51300480/download_file","bulk_download_file_name":"Glacial_landforms_and_Quaternary_landsca.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300480/Glacial_landforms_and_Quaternary_landsca20170111-6810-1gmlzqp-libre.pdf?1484140267=\u0026response-content-disposition=attachment%3B+filename%3DGlacial_landforms_and_Quaternary_landsca.pdf\u0026Expires=1743853385\u0026Signature=P3M7srlDghzgIrV3P15aF6V3o2ABJ46TPV538WxUhxFKvcN-8GZ-Ztdq96TN4g7~YeKSpunWdR-ayRAiHT9TNypsIAlV7TUwa44dMPwUL3u7jg97sayn5Dnp-tmqZ2pRbZs0k7OFP~hp40FTbujFaKl2FW51IL0VUpeDc-ResiEojSb9aAJ0Pfvn6m5K6ISASH9E1OboA27~2YfZq5LY~8IersQH~4w7cSt5cXyDBONWQzxXxNQUIgmOtx8wpqRkA8~FOHinsbU0xG6vPvmtELzLD~A2qmiRAXYjrlzO-zXSb~TMYsnNkC~4O96tg9PxZ-07qmlpZJTGYXkyBxpU6Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Glacial_landforms_and_Quaternary_landscape_development_in_Norway","translated_slug":"","page_count":23,"language":"en","content_type":"Work","summary":"The Norwegian landscape is a function of geological processes working over very long time spans, and first order structures might for example be traced to the ancient denudational processes, the Caledonian orogeny or break-up of the North Atlantic. However, a large portion of large-, intermediate-, and small-scale landforms in Norway owe their existence to Quaternary glaciations or periglacial processes. The Quaternary time period (the last c. 3 million years), is characterised by cool and variable climate with temperatures oscillating between relative mildness to frigid ice-age conditions. A wide spectrum of climate-driven geomorphological processes has thus been acting in Norway, but the numerous glaciations have had the most profound effect with the production of large U-shaped valleys, fjords and Alpine relief. On the other hand, interior and upland areas in Norway seem to be largely unaffected by glacial erosion and exhibit a possibly pre-Quaternary landscape with only some periglacial influence. The ice sheets in Scandinavia thus have redistributed rock mass and sediments in the landscape with the largest glaciogenic deposits being found on the continental shelf. Large Quaternary deposits and valley fills can also be found onshore and these are now valuable resources for aggregates, ground water and agriculture. Important Quaternary processes have also been acting along the Norwegian coast with denudation of the famous strandflat, where the formation processes are not fully understood. The isostatic depression of crust under the vast ice sheets have also lead to important consequences, with thick deposits of potentially unstable, fine-grained glaciomarine sediments in quite large areas of Norway. It is thus clear that much of Norway's beauty but also geohazard problems can be explained with the actions of Quaternary geomorphological processes.","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[{"id":51300480,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300480/thumbnails/1.jpg","file_name":"Glacial_landforms_and_Quaternary_landsca20170111-6810-1gmlzqp.pdf","download_url":"https://www.academia.edu/attachments/51300480/download_file","bulk_download_file_name":"Glacial_landforms_and_Quaternary_landsca.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300480/Glacial_landforms_and_Quaternary_landsca20170111-6810-1gmlzqp-libre.pdf?1484140267=\u0026response-content-disposition=attachment%3B+filename%3DGlacial_landforms_and_Quaternary_landsca.pdf\u0026Expires=1743853385\u0026Signature=P3M7srlDghzgIrV3P15aF6V3o2ABJ46TPV538WxUhxFKvcN-8GZ-Ztdq96TN4g7~YeKSpunWdR-ayRAiHT9TNypsIAlV7TUwa44dMPwUL3u7jg97sayn5Dnp-tmqZ2pRbZs0k7OFP~hp40FTbujFaKl2FW51IL0VUpeDc-ResiEojSb9aAJ0Pfvn6m5K6ISASH9E1OboA27~2YfZq5LY~8IersQH~4w7cSt5cXyDBONWQzxXxNQUIgmOtx8wpqRkA8~FOHinsbU0xG6vPvmtELzLD~A2qmiRAXYjrlzO-zXSb~TMYsnNkC~4O96tg9PxZ-07qmlpZJTGYXkyBxpU6Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874039-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874038"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874038/Nordic_seas_climate_variability_over_the_past_2_millennia_a_tropical_link"><img alt="Research paper thumbnail of Nordic seas climate variability over the past 2 millennia - a tropical link" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Nordic seas climate variability over the past 2 millennia - a tropical link</div><div class="wp-workCard_item"><span>Egs Agu Eug Joint Assembly</span><span>, Apr 1, 2003</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">High resolution records of mean annual and summer temperatures over the past 2 millennia have bee...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">High resolution records of mean annual and summer temperatures over the past 2 millennia have been developed for the Nordic Seas and adjacent land areas with decadal resolution. A new high quality age model for these records has been developed using a novel tree-ring correlation. The data show a very strong land-ocean coherence. Correlation to instrumental time series is also strong. A remarkable correspondance with proxy records of the nortward extent of the ITZC is apparent in the data, based on correlations to a rainfall/runoff proxy from Cariaco Basin off Venezuela. Further comparisons with long time series of North Atlantic indices based on instrumental data and proxy records are underway and will be reported. The strong tropical linkage is also noticeable in the instrumental time series, indicating possible tropical influence on decadal to century climate changes in the high latitude North Atlantic.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874038"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874038"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874038; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874038]").text(description); $(".js-view-count[data-work-id=30874038]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874038; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874038']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=30874038]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874038,"title":"Nordic seas climate variability over the past 2 millennia - a tropical link","translated_title":"","metadata":{"abstract":"High resolution records of mean annual and summer temperatures over the past 2 millennia have been developed for the Nordic Seas and adjacent land areas with decadal resolution. 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Jomelli</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/GregoryWiles">Gregory Wiles</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://ncsu.academia.edu/LewisOwen">Lewis A Owen</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://uib.academia.edu/AtleNesje">Atle Nesje</a>, and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/HodgsonDominic">Dominic Hodgson</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">A global overview of glacier advances and retreats (grouped by regions and by millennia) for the ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">A global overview of glacier advances and retreats (grouped by regions and by millennia) for the Holocene is compiled from previous studies. The reconstructions of glacier fluctuations are based on 1) mapping and dating moraines defined by 14 C, TCN, OSL, lichenometry and tree rings (discontinuous records/time series), and 2) sediments from proglacial lakes and speleothems (continuous records/ time series). Using 189 continuous and discontinuous time series, the long-term trends and centennial fluctuations of glaciers were compared to trends in the recession of Northern and mountain tree lines, and with orbital, solar and volcanic studies to examine the likely forcing factors that drove the changes recorded. A general trend of increasing glacier size from the earlyemid Holocene, to the late</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="4b9c23e02878a0de47d709dce89d193c" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":46331647,"asset_id":25981257,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/46331647/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="25981257"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="25981257"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 25981257; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=25981257]").text(description); $(".js-view-count[data-work-id=25981257]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 25981257; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='25981257']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "4b9c23e02878a0de47d709dce89d193c" } } $('.js-work-strip[data-work-id=25981257]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":25981257,"title":"Holocene glacier fluctuations","translated_title":"","metadata":{"abstract":"A global overview of glacier advances and retreats (grouped by regions and by millennia) for the Holocene is compiled from previous studies. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874036-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874035"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/30874035/Holocene_mean_July_temperature_and_winter_precipitation_in_western_Norway_inferred_from_lake_sediment_proxies"><img alt="Research paper thumbnail of Holocene mean July temperature and winter precipitation in western Norway inferred from lake sediment proxies" class="work-thumbnail" src="https://attachments.academia-assets.com/51300474/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/30874035/Holocene_mean_July_temperature_and_winter_precipitation_in_western_Norway_inferred_from_lake_sediment_proxies">Holocene mean July temperature and winter precipitation in western Norway inferred from lake sediment proxies</a></div><div class="wp-workCard_item"><span>The Holocene</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Reconstructions of mean July temperature (T jul ) and winter precipitation (P w ) for the last 11...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Reconstructions of mean July temperature (T jul ) and winter precipitation (P w ) for the last 11/500 years on the Folgefonna peninsula are presented. T jul was reconstructed using pollen Á/climate transfer functions and P w was reconstructed based on the exponential relationship between mean solid winter precipitation and ablation-season temperature at the equilibrium-line altitude (ELA) with a reconstructed former ELA, using T jul as the proxy for ablation-season temperature. The reconstructions from the Folgefonna peninsula suggest that the early Holocene was relatively cool and dry until c. 8000 cal. yr BP, followed by a warm and humid mid-Holocene until c. 4000 cal. yr BP with inferred T jul above 128C and P w reaching as high as 225% of the present day. Subsequent to c. 4000 cal. yr BP a reduction is seen in both inferred T jul and P w with large fluctuations during the last 500 years. In addition, new calculations of P w from two glaciers (Hardangerjøkulen and Jostedalsbreen) in southern Norway are presented. The results show that P w varied in phase at all glaciers, probably as a response to the same climate forcing factor. During the early Holocene a major shift is suggested between winds from the west and the east.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2b626bfa6982729c2b552c3fddedff48" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":51300474,"asset_id":30874035,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/51300474/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874035"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874035"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874035; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874035]").text(description); $(".js-view-count[data-work-id=30874035]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874035; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874035']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "2b626bfa6982729c2b552c3fddedff48" } } $('.js-work-strip[data-work-id=30874035]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874035,"title":"Holocene mean July temperature and winter precipitation in western Norway inferred from lake sediment proxies","translated_title":"","metadata":{"grobid_abstract":"Reconstructions of mean July temperature (T jul ) and winter precipitation (P w ) for the last 11/500 years on the Folgefonna peninsula are presented. T jul was reconstructed using pollen Á/climate transfer functions and P w was reconstructed based on the exponential relationship between mean solid winter precipitation and ablation-season temperature at the equilibrium-line altitude (ELA) with a reconstructed former ELA, using T jul as the proxy for ablation-season temperature. The reconstructions from the Folgefonna peninsula suggest that the early Holocene was relatively cool and dry until c. 8000 cal. yr BP, followed by a warm and humid mid-Holocene until c. 4000 cal. yr BP with inferred T jul above 128C and P w reaching as high as 225% of the present day. Subsequent to c. 4000 cal. yr BP a reduction is seen in both inferred T jul and P w with large fluctuations during the last 500 years. In addition, new calculations of P w from two glaciers (Hardangerjøkulen and Jostedalsbreen) in southern Norway are presented. The results show that P w varied in phase at all glaciers, probably as a response to the same climate forcing factor. 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T jul was reconstructed using pollen Á/climate transfer functions and P w was reconstructed based on the exponential relationship between mean solid winter precipitation and ablation-season temperature at the equilibrium-line altitude (ELA) with a reconstructed former ELA, using T jul as the proxy for ablation-season temperature. The reconstructions from the Folgefonna peninsula suggest that the early Holocene was relatively cool and dry until c. 8000 cal. yr BP, followed by a warm and humid mid-Holocene until c. 4000 cal. yr BP with inferred T jul above 128C and P w reaching as high as 225% of the present day. Subsequent to c. 4000 cal. yr BP a reduction is seen in both inferred T jul and P w with large fluctuations during the last 500 years. In addition, new calculations of P w from two glaciers (Hardangerjøkulen and Jostedalsbreen) in southern Norway are presented. The results show that P w varied in phase at all glaciers, probably as a response to the same climate forcing factor. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874032-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874031"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/30874031/Holocene_glacial_and_climate_history_of_the_Jostedalsbreen_region_Western_Norway_evidence_from_lake_sediments_and_terrestrial_deposits"><img alt="Research paper thumbnail of Holocene glacial and climate history of the Jostedalsbreen region, Western Norway; evidence from lake sediments and terrestrial deposits" class="work-thumbnail" src="https://attachments.academia-assets.com/51300471/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/30874031/Holocene_glacial_and_climate_history_of_the_Jostedalsbreen_region_Western_Norway_evidence_from_lake_sediments_and_terrestrial_deposits">Holocene glacial and climate history of the Jostedalsbreen region, Western Norway; evidence from lake sediments and terrestrial deposits</a></div><div class="wp-workCard_item"><span>Quaternary Science Reviews</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The valleys surroundingthe Jostedalsbreen ice cap were deglaciated during the latter half of the ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The valleys surroundingthe Jostedalsbreen ice cap were deglaciated during the latter half of the Preboreal Chronozone. At the end of the Preboreal Chronozone, however, a glacier readvance occurred. Terminal moraines were deposited by outlet valley glaciers from the Jostedalsbreen Plateau up to 1 km beyond Little Ice A~ge moraines. Inferred from the altitude of lateral moraines formed during this readvance and calculations of the equilibrium-line altitude (ELA) depression based on an accumulation area ratio (AAR) of 0.6, the average depression of the ELA was 325 +75/-115 m below the present. By assuming a similar precipitation pattern as at present, this suggests a mean temperature decline of about 2°C. Palynological investigations from Sygneskardet, Sunndalen, indicate that climate like the present was achieved just after 9000 BP. The Holocene climatic optimum occurred during the Atlantic Chronozone, with elm (Ulmus) stands growing at the present birch (Betula) forest limit in Sunndalen and pine (Pinus) growing at Styggevatnet to an altitude of at least 1160 m. Durin[g this period the mean summer temperature is estimated to have been at least 2.7 and 1.8°C warmer than at present, with and wtthout the local climatic effect of Jostedalsbreen, respectively. An inferred rise of the ELA of about 400 m from the present altitude suggests that possibly no glaciers existed on the Jostedalsbreen Plateau during the Holocene climatic optimum. Vegetational chan~es as deduced from palynological studies, lowered tree limits and increased resedimentation in peat bogs indicate general climatic deterioration since the Late Atlantic Chronozone.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="1dda190660f62119501b7ffa70db0dbc" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":51300471,"asset_id":30874031,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/51300471/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874031"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874031"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874031; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874031]").text(description); $(".js-view-count[data-work-id=30874031]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874031; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874031']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "1dda190660f62119501b7ffa70db0dbc" } } $('.js-work-strip[data-work-id=30874031]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874031,"title":"Holocene glacial and climate history of the Jostedalsbreen region, Western Norway; evidence from lake sediments and terrestrial deposits","translated_title":"","metadata":{"ai_title_tag":"Holocene Climate and Glacial History of Jostedalsbreen","grobid_abstract":"The valleys surroundingthe Jostedalsbreen ice cap were deglaciated during the latter half of the Preboreal Chronozone. At the end of the Preboreal Chronozone, however, a glacier readvance occurred. Terminal moraines were deposited by outlet valley glaciers from the Jostedalsbreen Plateau up to 1 km beyond Little Ice A~ge moraines. Inferred from the altitude of lateral moraines formed during this readvance and calculations of the equilibrium-line altitude (ELA) depression based on an accumulation area ratio (AAR) of 0.6, the average depression of the ELA was 325 +75/-115 m below the present. By assuming a similar precipitation pattern as at present, this suggests a mean temperature decline of about 2°C. Palynological investigations from Sygneskardet, Sunndalen, indicate that climate like the present was achieved just after 9000 BP. The Holocene climatic optimum occurred during the Atlantic Chronozone, with elm (Ulmus) stands growing at the present birch (Betula) forest limit in Sunndalen and pine (Pinus) growing at Styggevatnet to an altitude of at least 1160 m. Durin[g this period the mean summer temperature is estimated to have been at least 2.7 and 1.8°C warmer than at present, with and wtthout the local climatic effect of Jostedalsbreen, respectively. An inferred rise of the ELA of about 400 m from the present altitude suggests that possibly no glaciers existed on the Jostedalsbreen Plateau during the Holocene climatic optimum. Vegetational chan~es as deduced from palynological studies, lowered tree limits and increased resedimentation in peat bogs indicate general climatic deterioration since the Late Atlantic Chronozone.","publication_name":"Quaternary Science Reviews","grobid_abstract_attachment_id":51300471},"translated_abstract":null,"internal_url":"https://www.academia.edu/30874031/Holocene_glacial_and_climate_history_of_the_Jostedalsbreen_region_Western_Norway_evidence_from_lake_sediments_and_terrestrial_deposits","translated_internal_url":"","created_at":"2017-01-11T05:01:28.434-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":51300471,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300471/thumbnails/1.jpg","file_name":"Holocene_glacial_and_climate_history_of_20170111-6810-17x38bn.pdf","download_url":"https://www.academia.edu/attachments/51300471/download_file","bulk_download_file_name":"Holocene_glacial_and_climate_history_of.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300471/Holocene_glacial_and_climate_history_of_20170111-6810-17x38bn-libre.pdf?1484140105=\u0026response-content-disposition=attachment%3B+filename%3DHolocene_glacial_and_climate_history_of.pdf\u0026Expires=1743853387\u0026Signature=e~A880Cqd9dWh9ngMN4ejUu3NLTix3eSHTWo0QKZSIPjcz0kD~noUM-nYL9F9e0bwqU0MArZE39b86Ev-FLsty4ON8r5Ugwu4XhamHbQvfC8RdkbSyPxmR8pk-tsIavYctxNwX2r32MUfFO4rNz1Hhz3eeLSFwRvCN4XWjxy7Rm-d-ebMUg-foAv0cQgHceN~iBNngEOrOoWr4CnIFrPSU35BrbmJcrENFE5iw83zsQ1~UZ8c-g4B0aVToRI-Djku01wC13TmFX-nYqGYfMQQ-d1t6Cg2Tc60cGXTvpgpHHnGNBj67PRzw97qae-TI0nHtZbt7DJtScV0JxVVDdNnw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Holocene_glacial_and_climate_history_of_the_Jostedalsbreen_region_Western_Norway_evidence_from_lake_sediments_and_terrestrial_deposits","translated_slug":"","page_count":29,"language":"en","content_type":"Work","summary":"The valleys surroundingthe Jostedalsbreen ice cap were deglaciated during the latter half of the Preboreal Chronozone. At the end of the Preboreal Chronozone, however, a glacier readvance occurred. Terminal moraines were deposited by outlet valley glaciers from the Jostedalsbreen Plateau up to 1 km beyond Little Ice A~ge moraines. Inferred from the altitude of lateral moraines formed during this readvance and calculations of the equilibrium-line altitude (ELA) depression based on an accumulation area ratio (AAR) of 0.6, the average depression of the ELA was 325 +75/-115 m below the present. By assuming a similar precipitation pattern as at present, this suggests a mean temperature decline of about 2°C. Palynological investigations from Sygneskardet, Sunndalen, indicate that climate like the present was achieved just after 9000 BP. The Holocene climatic optimum occurred during the Atlantic Chronozone, with elm (Ulmus) stands growing at the present birch (Betula) forest limit in Sunndalen and pine (Pinus) growing at Styggevatnet to an altitude of at least 1160 m. Durin[g this period the mean summer temperature is estimated to have been at least 2.7 and 1.8°C warmer than at present, with and wtthout the local climatic effect of Jostedalsbreen, respectively. An inferred rise of the ELA of about 400 m from the present altitude suggests that possibly no glaciers existed on the Jostedalsbreen Plateau during the Holocene climatic optimum. Vegetational chan~es as deduced from palynological studies, lowered tree limits and increased resedimentation in peat bogs indicate general climatic deterioration since the Late Atlantic Chronozone.","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[{"id":51300471,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300471/thumbnails/1.jpg","file_name":"Holocene_glacial_and_climate_history_of_20170111-6810-17x38bn.pdf","download_url":"https://www.academia.edu/attachments/51300471/download_file","bulk_download_file_name":"Holocene_glacial_and_climate_history_of.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300471/Holocene_glacial_and_climate_history_of_20170111-6810-17x38bn-libre.pdf?1484140105=\u0026response-content-disposition=attachment%3B+filename%3DHolocene_glacial_and_climate_history_of.pdf\u0026Expires=1743853387\u0026Signature=e~A880Cqd9dWh9ngMN4ejUu3NLTix3eSHTWo0QKZSIPjcz0kD~noUM-nYL9F9e0bwqU0MArZE39b86Ev-FLsty4ON8r5Ugwu4XhamHbQvfC8RdkbSyPxmR8pk-tsIavYctxNwX2r32MUfFO4rNz1Hhz3eeLSFwRvCN4XWjxy7Rm-d-ebMUg-foAv0cQgHceN~iBNngEOrOoWr4CnIFrPSU35BrbmJcrENFE5iw83zsQ1~UZ8c-g4B0aVToRI-Djku01wC13TmFX-nYqGYfMQQ-d1t6Cg2Tc60cGXTvpgpHHnGNBj67PRzw97qae-TI0nHtZbt7DJtScV0JxVVDdNnw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":93755,"name":"History and archaeology","url":"https://www.academia.edu/Documents/in/History_and_archaeology"},{"id":373417,"name":"Quaternary Science Reviews","url":"https://www.academia.edu/Documents/in/Quaternary_Science_Reviews"}],"urls":[]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874029-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874028"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874028/The_Expression_of_the_8_2_ka_and_Younger_Dryas_Events_in_the_Eastern_Canadian_Arctic"><img alt="Research paper thumbnail of The Expression of the 8.2 ka and Younger Dryas Events in the Eastern Canadian Arctic" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">The Expression of the 8.2 ka and Younger Dryas Events in the Eastern Canadian Arctic</div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The two largest climate coolings following the end of the last glaciation are the Younger Dryas a...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The two largest climate coolings following the end of the last glaciation are the Younger Dryas and the 8.2 ka events. Evidence for these cold excursions is widespread around the North Atlantic and in more distant regions. Both events are well expressed in Greenland ice cores; glacier readvances occurred across much of NW Europe during the Younger Dryas and cold surface waters returned to the North Atlantic, with depressed summer temperatures in eastern North America. The 8.2 ka event has a similar pattern, but the magnitude is substantially lower, with a much shorter duration. However, surprisingly little evidence has been presented for either event from the North Atlantic Arctic. Recently acquired lake sediment records from the Eastern Canadian Arctic contain evidence for both excursions. The 8.2 ka event is recorded at two sites as a significant glacier readvance of cirque and outlet glaciers of local ice caps at 8.2±0.1 ka. In some non-glacially-dominated lakes, a reduction in primary productivity is apparent at the same time. These records suggest colder summers without a dramatic reduction in precipitation, producing positive mass balances and glacier readvances. For most local glaciers, this was the last significant readvance before they receded behind their Little Ice Age margins. Only a few lakes contain records that extend through the Younger Dryas chron. The best-dated lake record, Donard Lake, extends back to 15 ka. Lacustrine sedimentation is currently dominated by a meltwater from an outlet glacier that terminates a few hundred meters from the lake. The glacier has been within the drainage basin of the lake for the past 5.5 ka, although the contribution of glacial sediment has been larger since about 2.5 ka. Prior to 5.5 ka, there is no evidence of a glacier in the catchment of Donard Lake, suggesting that throughout the entire Neoglacial period, the local glacier has been more advanced than at any time since 15 ka. During the Younger Dryas chron, lacustrine primary productivity was greatly reduced, whether measured as the flux of organic carbon to the lake floor or as the percentage of organic matter in lake sediment. We interpret this change to reflect a substantial reduction in summer temperatures for more than 1 ka. However, this temperature drop was not accompanied by a significant glacier readvance, suggesting precipitation must have been very low. This differs from the 8.2 ka event when precipitation must have remained relatively high. These records indicate that in the Eastern Canadian Arctic, summers during the Younger Dryas were much colder than present, but precipitation was dramatically lower too, so glaciers did not advance, whereas during the briefer, and less severe summer cooling associated with the 8.2 ka event, precipitation was not dramatically reduced and glaciers readvanced.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874028"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874028"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874028; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874028]").text(description); $(".js-view-count[data-work-id=30874028]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874028; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874028']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=30874028]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874028,"title":"The Expression of the 8.2 ka and Younger Dryas Events in the Eastern Canadian Arctic","translated_title":"","metadata":{"abstract":"The two largest climate coolings following the end of the last glaciation are the Younger Dryas and the 8.2 ka events. Evidence for these cold excursions is widespread around the North Atlantic and in more distant regions. Both events are well expressed in Greenland ice cores; glacier readvances occurred across much of NW Europe during the Younger Dryas and cold surface waters returned to the North Atlantic, with depressed summer temperatures in eastern North America. The 8.2 ka event has a similar pattern, but the magnitude is substantially lower, with a much shorter duration. However, surprisingly little evidence has been presented for either event from the North Atlantic Arctic. Recently acquired lake sediment records from the Eastern Canadian Arctic contain evidence for both excursions. The 8.2 ka event is recorded at two sites as a significant glacier readvance of cirque and outlet glaciers of local ice caps at 8.2±0.1 ka. In some non-glacially-dominated lakes, a reduction in primary productivity is apparent at the same time. These records suggest colder summers without a dramatic reduction in precipitation, producing positive mass balances and glacier readvances. For most local glaciers, this was the last significant readvance before they receded behind their Little Ice Age margins. Only a few lakes contain records that extend through the Younger Dryas chron. The best-dated lake record, Donard Lake, extends back to 15 ka. Lacustrine sedimentation is currently dominated by a meltwater from an outlet glacier that terminates a few hundred meters from the lake. The glacier has been within the drainage basin of the lake for the past 5.5 ka, although the contribution of glacial sediment has been larger since about 2.5 ka. Prior to 5.5 ka, there is no evidence of a glacier in the catchment of Donard Lake, suggesting that throughout the entire Neoglacial period, the local glacier has been more advanced than at any time since 15 ka. During the Younger Dryas chron, lacustrine primary productivity was greatly reduced, whether measured as the flux of organic carbon to the lake floor or as the percentage of organic matter in lake sediment. We interpret this change to reflect a substantial reduction in summer temperatures for more than 1 ka. However, this temperature drop was not accompanied by a significant glacier readvance, suggesting precipitation must have been very low. This differs from the 8.2 ka event when precipitation must have remained relatively high. These records indicate that in the Eastern Canadian Arctic, summers during the Younger Dryas were much colder than present, but precipitation was dramatically lower too, so glaciers did not advance, whereas during the briefer, and less severe summer cooling associated with the 8.2 ka event, precipitation was not dramatically reduced and glaciers readvanced."},"translated_abstract":"The two largest climate coolings following the end of the last glaciation are the Younger Dryas and the 8.2 ka events. Evidence for these cold excursions is widespread around the North Atlantic and in more distant regions. Both events are well expressed in Greenland ice cores; glacier readvances occurred across much of NW Europe during the Younger Dryas and cold surface waters returned to the North Atlantic, with depressed summer temperatures in eastern North America. The 8.2 ka event has a similar pattern, but the magnitude is substantially lower, with a much shorter duration. However, surprisingly little evidence has been presented for either event from the North Atlantic Arctic. Recently acquired lake sediment records from the Eastern Canadian Arctic contain evidence for both excursions. The 8.2 ka event is recorded at two sites as a significant glacier readvance of cirque and outlet glaciers of local ice caps at 8.2±0.1 ka. In some non-glacially-dominated lakes, a reduction in primary productivity is apparent at the same time. These records suggest colder summers without a dramatic reduction in precipitation, producing positive mass balances and glacier readvances. For most local glaciers, this was the last significant readvance before they receded behind their Little Ice Age margins. Only a few lakes contain records that extend through the Younger Dryas chron. The best-dated lake record, Donard Lake, extends back to 15 ka. Lacustrine sedimentation is currently dominated by a meltwater from an outlet glacier that terminates a few hundred meters from the lake. The glacier has been within the drainage basin of the lake for the past 5.5 ka, although the contribution of glacial sediment has been larger since about 2.5 ka. Prior to 5.5 ka, there is no evidence of a glacier in the catchment of Donard Lake, suggesting that throughout the entire Neoglacial period, the local glacier has been more advanced than at any time since 15 ka. During the Younger Dryas chron, lacustrine primary productivity was greatly reduced, whether measured as the flux of organic carbon to the lake floor or as the percentage of organic matter in lake sediment. We interpret this change to reflect a substantial reduction in summer temperatures for more than 1 ka. However, this temperature drop was not accompanied by a significant glacier readvance, suggesting precipitation must have been very low. This differs from the 8.2 ka event when precipitation must have remained relatively high. These records indicate that in the Eastern Canadian Arctic, summers during the Younger Dryas were much colder than present, but precipitation was dramatically lower too, so glaciers did not advance, whereas during the briefer, and less severe summer cooling associated with the 8.2 ka event, precipitation was not dramatically reduced and glaciers readvanced.","internal_url":"https://www.academia.edu/30874028/The_Expression_of_the_8_2_ka_and_Younger_Dryas_Events_in_the_Eastern_Canadian_Arctic","translated_internal_url":"","created_at":"2017-01-11T05:01:27.009-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"The_Expression_of_the_8_2_ka_and_Younger_Dryas_Events_in_the_Eastern_Canadian_Arctic","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"The two largest climate coolings following the end of the last glaciation are the Younger Dryas and the 8.2 ka events. 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These records suggest colder summers without a dramatic reduction in precipitation, producing positive mass balances and glacier readvances. For most local glaciers, this was the last significant readvance before they receded behind their Little Ice Age margins. Only a few lakes contain records that extend through the Younger Dryas chron. The best-dated lake record, Donard Lake, extends back to 15 ka. Lacustrine sedimentation is currently dominated by a meltwater from an outlet glacier that terminates a few hundred meters from the lake. The glacier has been within the drainage basin of the lake for the past 5.5 ka, although the contribution of glacial sediment has been larger since about 2.5 ka. Prior to 5.5 ka, there is no evidence of a glacier in the catchment of Donard Lake, suggesting that throughout the entire Neoglacial period, the local glacier has been more advanced than at any time since 15 ka. During the Younger Dryas chron, lacustrine primary productivity was greatly reduced, whether measured as the flux of organic carbon to the lake floor or as the percentage of organic matter in lake sediment. We interpret this change to reflect a substantial reduction in summer temperatures for more than 1 ka. However, this temperature drop was not accompanied by a significant glacier readvance, suggesting precipitation must have been very low. This differs from the 8.2 ka event when precipitation must have remained relatively high. These records indicate that in the Eastern Canadian Arctic, summers during the Younger Dryas were much colder than present, but precipitation was dramatically lower too, so glaciers did not advance, whereas during the briefer, and less severe summer cooling associated with the 8.2 ka event, precipitation was not dramatically reduced and glaciers readvanced.","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[],"research_interests":[{"id":42073,"name":"North Eastern North America Archaeology","url":"https://www.academia.edu/Documents/in/North_Eastern_North_America_Archaeology"},{"id":82675,"name":"North Atlantic","url":"https://www.academia.edu/Documents/in/North_Atlantic"},{"id":142810,"name":"Surface Water","url":"https://www.academia.edu/Documents/in/Surface_Water"},{"id":152776,"name":"Younger Dryas","url":"https://www.academia.edu/Documents/in/Younger_Dryas"},{"id":182364,"name":"Little Ice Age","url":"https://www.academia.edu/Documents/in/Little_Ice_Age"},{"id":198868,"name":"Ice Cores","url":"https://www.academia.edu/Documents/in/Ice_Cores"},{"id":289852,"name":"Primary Production","url":"https://www.academia.edu/Documents/in/Primary_Production"},{"id":585192,"name":"Organic carbon","url":"https://www.academia.edu/Documents/in/Organic_carbon"},{"id":970387,"name":"Organic Matter","url":"https://www.academia.edu/Documents/in/Organic_Matter"},{"id":1707373,"name":"Mass Balance","url":"https://www.academia.edu/Documents/in/Mass_Balance"},{"id":2196834,"name":"Canadian Arctic","url":"https://www.academia.edu/Documents/in/Canadian_Arctic"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874028-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874027"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874027/Holocene_Changes_in_Atmospherical_Circulation_in_the_North_Atlantic_Region_Evidences_for_Millennial_Scale_coVariability_Between_Ocean_and_Atmosphere_Circulation"><img alt="Research paper thumbnail of Holocene Changes in Atmospherical Circulation in the North Atlantic Region - Evidences for Millennial-Scale coVariability Between Ocean and Atmosphere Circulation" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Holocene Changes in Atmospherical Circulation in the North Atlantic Region - Evidences for Millennial-Scale coVariability Between Ocean and Atmosphere Circulation</div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Whereas a number of records from the marine realm have demonstrated Holocene changes regarded to ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Whereas a number of records from the marine realm have demonstrated Holocene changes regarded to be related to overturning circulation in the North Atlantic region, independent information of atmospherical variability from the terrestrial realm have proven more elusive to capture in palaeo-records. This is a major concern, as several studies have suggested that atmospherical forcing may be an important factor</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874027"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874027"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874027; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874027]").text(description); $(".js-view-count[data-work-id=30874027]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874027; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874027']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=30874027]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874027,"title":"Holocene Changes in Atmospherical Circulation in the North Atlantic Region - Evidences for Millennial-Scale coVariability Between Ocean and Atmosphere Circulation","translated_title":"","metadata":{"abstract":"Whereas a number of records from the marine realm have demonstrated Holocene changes regarded to be related to overturning circulation in the North Atlantic region, independent information of atmospherical variability from the terrestrial realm have proven more elusive to capture in palaeo-records. 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This is a major concern, as several studies have suggested that atmospherical forcing may be an important factor","internal_url":"https://www.academia.edu/30874027/Holocene_Changes_in_Atmospherical_Circulation_in_the_North_Atlantic_Region_Evidences_for_Millennial_Scale_coVariability_Between_Ocean_and_Atmosphere_Circulation","translated_internal_url":"","created_at":"2017-01-11T05:01:26.529-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Holocene_Changes_in_Atmospherical_Circulation_in_the_North_Atlantic_Region_Evidences_for_Millennial_Scale_coVariability_Between_Ocean_and_Atmosphere_Circulation","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Whereas a number of records from the marine realm have demonstrated Holocene changes regarded to be related to overturning circulation in the North Atlantic region, independent information of atmospherical variability from the terrestrial realm have proven more elusive to capture in palaeo-records. This is a major concern, as several studies have suggested that atmospherical forcing may be an important factor","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[],"research_interests":[{"id":30441,"name":"North Atlantic Ocean","url":"https://www.academia.edu/Documents/in/North_Atlantic_Ocean"},{"id":44265,"name":"North Atlantic Oscillation","url":"https://www.academia.edu/Documents/in/North_Atlantic_Oscillation"},{"id":62729,"name":"Air flow","url":"https://www.academia.edu/Documents/in/Air_flow"},{"id":82675,"name":"North Atlantic","url":"https://www.academia.edu/Documents/in/North_Atlantic"},{"id":113239,"name":"Ocean Circulation","url":"https://www.academia.edu/Documents/in/Ocean_Circulation"},{"id":150013,"name":"Late Holocene","url":"https://www.academia.edu/Documents/in/Late_Holocene"},{"id":236377,"name":"Spatial Distribution","url":"https://www.academia.edu/Documents/in/Spatial_Distribution"},{"id":303826,"name":"Atmospheric Circulation","url":"https://www.academia.edu/Documents/in/Atmospheric_Circulation"},{"id":314103,"name":"Inverse Modeling","url":"https://www.academia.edu/Documents/in/Inverse_Modeling"},{"id":2516014,"name":"temporal variation","url":"https://www.academia.edu/Documents/in/temporal_variation"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874027-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874026"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/30874026/Holocene_glacial_and_colluvial_activity_in_Leirungsdalen_eastern_Jotunheimen_south_central_Norway"><img alt="Research paper thumbnail of Holocene glacial and colluvial activity in Leirungsdalen, eastern Jotunheimen, south-central Norway" class="work-thumbnail" src="https://attachments.academia-assets.com/51300462/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/30874026/Holocene_glacial_and_colluvial_activity_in_Leirungsdalen_eastern_Jotunheimen_south_central_Norway">Holocene glacial and colluvial activity in Leirungsdalen, eastern Jotunheimen, south-central Norway</a></div><div class="wp-workCard_item"><span>Norsk Geologisk Tidsskrift</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Two terrestrial sections have been studied in order to reconstruct the Holocene glacial and collu...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Two terrestrial sections have been studied in order to reconstruct the Holocene glacial and colluvial history in Leirungsdalen, eastern Jotunheimen. The interpretation of individual sedimentary units is based on the grain-size distribution and compared with modern analogue samples collected in the respective streams and at sites close to the present glaciers. Stages of enhanced debris flow or glacial activity are recognized as sand and silt layers, respectively, while periods of low colluvial and glacial activity in the catchment are characterised by continuous peat accumulation. Age/depth curves based on radiocarbon dates from the Svarthammarbu and Steinflybekken sections indicate debris flow activity &gt; 7500, 7300-6800,6600-5500, 5800, 5700, 5300-4900,4700, 4500,4300, 2300, 2100-1500, 1300, 700-600 and 500-400 cal. yr BP. The first Holocene glacial signal is detected ca. 5300 cal. yr BP. The frequency of glacial events seems to have increased during the Late Holocene, especially...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d5b96cb3db7fcf5a11208098f5d18905" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":51300462,"asset_id":30874026,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/51300462/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874026"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874026"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874026; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874026]").text(description); $(".js-view-count[data-work-id=30874026]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874026; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874026']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d5b96cb3db7fcf5a11208098f5d18905" } } $('.js-work-strip[data-work-id=30874026]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874026,"title":"Holocene glacial and colluvial activity in Leirungsdalen, eastern Jotunheimen, south-central Norway","translated_title":"","metadata":{"abstract":"Two terrestrial sections have been studied in order to reconstruct the Holocene glacial and colluvial history in Leirungsdalen, eastern Jotunheimen. The interpretation of individual sedimentary units is based on the grain-size distribution and compared with modern analogue samples collected in the respective streams and at sites close to the present glaciers. Stages of enhanced debris flow or glacial activity are recognized as sand and silt layers, respectively, while periods of low colluvial and glacial activity in the catchment are characterised by continuous peat accumulation. Age/depth curves based on radiocarbon dates from the Svarthammarbu and Steinflybekken sections indicate debris flow activity \u0026gt; 7500, 7300-6800,6600-5500, 5800, 5700, 5300-4900,4700, 4500,4300, 2300, 2100-1500, 1300, 700-600 and 500-400 cal. yr BP. The first Holocene glacial signal is detected ca. 5300 cal. yr BP. The frequency of glacial events seems to have increased during the Late Holocene, especially...","ai_title_tag":"Holocene Glacial History in Leirungsdalen","publication_name":"Norsk Geologisk Tidsskrift"},"translated_abstract":"Two terrestrial sections have been studied in order to reconstruct the Holocene glacial and colluvial history in Leirungsdalen, eastern Jotunheimen. The interpretation of individual sedimentary units is based on the grain-size distribution and compared with modern analogue samples collected in the respective streams and at sites close to the present glaciers. Stages of enhanced debris flow or glacial activity are recognized as sand and silt layers, respectively, while periods of low colluvial and glacial activity in the catchment are characterised by continuous peat accumulation. Age/depth curves based on radiocarbon dates from the Svarthammarbu and Steinflybekken sections indicate debris flow activity \u0026gt; 7500, 7300-6800,6600-5500, 5800, 5700, 5300-4900,4700, 4500,4300, 2300, 2100-1500, 1300, 700-600 and 500-400 cal. yr BP. The first Holocene glacial signal is detected ca. 5300 cal. yr BP. The frequency of glacial events seems to have increased during the Late Holocene, especially...","internal_url":"https://www.academia.edu/30874026/Holocene_glacial_and_colluvial_activity_in_Leirungsdalen_eastern_Jotunheimen_south_central_Norway","translated_internal_url":"","created_at":"2017-01-11T05:01:25.989-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":51300462,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300462/thumbnails/1.jpg","file_name":"Holocene_glacial_and_colluvial_activity_20170111-6813-108sp5p.pdf","download_url":"https://www.academia.edu/attachments/51300462/download_file","bulk_download_file_name":"Holocene_glacial_and_colluvial_activity.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300462/Holocene_glacial_and_colluvial_activity_20170111-6813-108sp5p-libre.pdf?1484140117=\u0026response-content-disposition=attachment%3B+filename%3DHolocene_glacial_and_colluvial_activity.pdf\u0026Expires=1743853388\u0026Signature=ACiLdVjfr7Z-1rfBC73--WuzRNY9pxqZB8hP~26HdzOHaCmb50qQ0nvE2qnjKndSphELvR5PSs5CvIdETPznrIjA1QqomHHHb9Gu7KxeEBufG1paWAfarK9m0d0cbOwzddAt6~pvwHr5Wp3Cw-Q8AeaVt22CzV4096doLanlcZBUYUVVOulRf4kFlH~rEyfCra~ZykmhAtdWXBGM9XP1egxEQUrigHXyPEoi6CNnaO9J-6UwWZLMYiIDF5GLreA9yZW9OBWswBSrTDzg5-Retsh~HBCON0yOj9fqz3QbU4OA9ITt1SoDmwtgV1xHwfu2a6LAwogyVtduvtUif~GHuA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Holocene_glacial_and_colluvial_activity_in_Leirungsdalen_eastern_Jotunheimen_south_central_Norway","translated_slug":"","page_count":17,"language":"en","content_type":"Work","summary":"Two terrestrial sections have been studied in order to reconstruct the Holocene glacial and colluvial history in Leirungsdalen, eastern Jotunheimen. The interpretation of individual sedimentary units is based on the grain-size distribution and compared with modern analogue samples collected in the respective streams and at sites close to the present glaciers. Stages of enhanced debris flow or glacial activity are recognized as sand and silt layers, respectively, while periods of low colluvial and glacial activity in the catchment are characterised by continuous peat accumulation. Age/depth curves based on radiocarbon dates from the Svarthammarbu and Steinflybekken sections indicate debris flow activity \u0026gt; 7500, 7300-6800,6600-5500, 5800, 5700, 5300-4900,4700, 4500,4300, 2300, 2100-1500, 1300, 700-600 and 500-400 cal. yr BP. The first Holocene glacial signal is detected ca. 5300 cal. yr BP. The frequency of glacial events seems to have increased during the Late Holocene, especially...","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[{"id":51300462,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300462/thumbnails/1.jpg","file_name":"Holocene_glacial_and_colluvial_activity_20170111-6813-108sp5p.pdf","download_url":"https://www.academia.edu/attachments/51300462/download_file","bulk_download_file_name":"Holocene_glacial_and_colluvial_activity.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300462/Holocene_glacial_and_colluvial_activity_20170111-6813-108sp5p-libre.pdf?1484140117=\u0026response-content-disposition=attachment%3B+filename%3DHolocene_glacial_and_colluvial_activity.pdf\u0026Expires=1743853388\u0026Signature=ACiLdVjfr7Z-1rfBC73--WuzRNY9pxqZB8hP~26HdzOHaCmb50qQ0nvE2qnjKndSphELvR5PSs5CvIdETPznrIjA1QqomHHHb9Gu7KxeEBufG1paWAfarK9m0d0cbOwzddAt6~pvwHr5Wp3Cw-Q8AeaVt22CzV4096doLanlcZBUYUVVOulRf4kFlH~rEyfCra~ZykmhAtdWXBGM9XP1egxEQUrigHXyPEoi6CNnaO9J-6UwWZLMYiIDF5GLreA9yZW9OBWswBSrTDzg5-Retsh~HBCON0yOj9fqz3QbU4OA9ITt1SoDmwtgV1xHwfu2a6LAwogyVtduvtUif~GHuA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874026-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874025"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874025/Time_Series_at_Decadal_Resolution_Show_Tropical_Influence_on_Climate_Variability_in_The_Eastern_Nordic_Seas_Over_the_Past_2_Millenia"><img alt="Research paper thumbnail of Time Series at Decadal Resolution Show Tropical Influence on Climate Variability in The Eastern Nordic Seas Over the Past 2 Millenia" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Time Series at Decadal Resolution Show Tropical Influence on Climate Variability in The Eastern Nordic Seas Over the Past 2 Millenia</div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Multi-proxy paleoclimatic time series have been developed from IMAGES Sites and adjacent suppleme...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Multi-proxy paleoclimatic time series have been developed from IMAGES Sites and adjacent supplementary cores in the Eastern Norwegian Sea. The records cover the last 2000 years at decadal resolution, allowing for a detailed reconstruction of the surface hydrography of the main path of the northern limb of the north Atlantic circulation cell. Centennial to millennial scale events are recorded, such as the &quot;Medieval Warm Phase&quot; (MWP) and the &quot;Little Ice Age&quot; (LIA), which constitute the main long term century scale features. Superimposed on these are multidecadal variability of somewhat less amplitude. There is a close correspondance with continental records reflecting summer temperaure and winter precipitation in western Scandinavia over this period.SST changes are found to be in the range of 1-2 degrees. Significant land-sea correlation is observed. A cold phase in the early 20th Century, a series of cold phases in the LIA and two warm phases in the MWP are observ...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874025"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874025"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874025; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874025]").text(description); $(".js-view-count[data-work-id=30874025]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874025; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874025']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=30874025]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874025,"title":"Time Series at Decadal Resolution Show Tropical Influence on Climate Variability in The Eastern Nordic Seas Over the Past 2 Millenia","translated_title":"","metadata":{"abstract":"Multi-proxy paleoclimatic time series have been developed from IMAGES Sites and adjacent supplementary cores in the Eastern Norwegian Sea. 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Significant land-sea correlation is observed. A cold phase in the early 20th Century, a series of cold phases in the LIA and two warm phases in the MWP are observ...","internal_url":"https://www.academia.edu/30874025/Time_Series_at_Decadal_Resolution_Show_Tropical_Influence_on_Climate_Variability_in_The_Eastern_Nordic_Seas_Over_the_Past_2_Millenia","translated_internal_url":"","created_at":"2017-01-11T05:01:25.461-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Time_Series_at_Decadal_Resolution_Show_Tropical_Influence_on_Climate_Variability_in_The_Eastern_Nordic_Seas_Over_the_Past_2_Millenia","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Multi-proxy paleoclimatic time series have been developed from IMAGES Sites and adjacent supplementary cores in the Eastern Norwegian Sea. 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BP in the Smørstabbtinden massif of central Jotunheimen, southern Norway. Particular attention is paid to the century- to millennial-scale, pre-Little Ice Age glacial signal based on an estimated temporal resolution of ⩽55 and ⩽25 yr cm−1 for Bøvertunsvatnet and Dalsvatnet, respectively. Visible lithostratigraphic variations, organic content/loss-on-ignition, calcium carbonate content, magnetic susceptibility and grain-size fractions (especially the fine silt) are used as proxy indicators of glacier presence and extent in the lake catchments.Following deglaciation, the early Holocene was characterized by generally small glaciers until a major advance (the Finse Event) peaking at approximately 8200 cal. BP. From 7900 to at least 5300 cal. BP glaciers appear to have been absent from central Jotunheimen. There is evidence of glacier expansion between about...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="efbc5b648b0f6c8ae6bc85406a80c6c6" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":51300464,"asset_id":30874024,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/51300464/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874024"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874024"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874024; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874024]").text(description); $(".js-view-count[data-work-id=30874024]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874024; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874024']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "efbc5b648b0f6c8ae6bc85406a80c6c6" } } $('.js-work-strip[data-work-id=30874024]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874024,"title":"Holocene glacier variations in central Jotunheimen, southern Norway based on distal glaciolacustrine sediment cores","translated_title":"","metadata":{"abstract":"Sediment cores from two glacier-fed lakes are used to reconstruct a continuous record of glacier variations since about 10,000 cal. 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There is evidence of glacier expansion between about...","internal_url":"https://www.academia.edu/30874024/Holocene_glacier_variations_in_central_Jotunheimen_southern_Norway_based_on_distal_glaciolacustrine_sediment_cores","translated_internal_url":"","created_at":"2017-01-11T05:01:24.935-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":51300464,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300464/thumbnails/1.jpg","file_name":"Holocene_glacier_variations_in_central_J20170111-6807-jkj07j.pdf","download_url":"https://www.academia.edu/attachments/51300464/download_file","bulk_download_file_name":"Holocene_glacier_variations_in_central_J.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300464/Holocene_glacier_variations_in_central_J20170111-6807-jkj07j-libre.pdf?1484140093=\u0026response-content-disposition=attachment%3B+filename%3DHolocene_glacier_variations_in_central_J.pdf\u0026Expires=1743853388\u0026Signature=V0Qcjj4sADzukWqvWwVpgU0HOOQpiEuOmJ~YrO4BF26SJ95YG0FjnzOrWJ8hx1LVWKlxncH0JxIdmi6~HXgajg2UIWxZEDxEkr8TLgOrwdV2vPihDvVPUF~2MM-DrMke8ipJqqKSLd8BJG39712LaMozts9JWSOLSHtEtYW6fBC8giU-~8I~kCwORItSHEzsGrbFEUYK5xzVDczF5A~I47mOjRASdpZ6-IAH8uFVRB2~WrKyG5bp2wZJswKY4NdWmGECvK8QqUH4B7tEPxI1LhM9iW1OaeqN-T4OH~YFkRPcukFyAsBzU2VtdzcD9wH3QHuZ~XOcOh9VMso~nZ5wtg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Holocene_glacier_variations_in_central_Jotunheimen_southern_Norway_based_on_distal_glaciolacustrine_sediment_cores","translated_slug":"","page_count":24,"language":"en","content_type":"Work","summary":"Sediment cores from two glacier-fed lakes are used to reconstruct a continuous record of glacier variations since about 10,000 cal. BP in the Smørstabbtinden massif of central Jotunheimen, southern Norway. Particular attention is paid to the century- to millennial-scale, pre-Little Ice Age glacial signal based on an estimated temporal resolution of ⩽55 and ⩽25 yr cm−1 for Bøvertunsvatnet and Dalsvatnet, respectively. Visible lithostratigraphic variations, organic content/loss-on-ignition, calcium carbonate content, magnetic susceptibility and grain-size fractions (especially the fine silt) are used as proxy indicators of glacier presence and extent in the lake catchments.Following deglaciation, the early Holocene was characterized by generally small glaciers until a major advance (the Finse Event) peaking at approximately 8200 cal. BP. From 7900 to at least 5300 cal. BP glaciers appear to have been absent from central Jotunheimen. There is evidence of glacier expansion between about...","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[{"id":51300464,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300464/thumbnails/1.jpg","file_name":"Holocene_glacier_variations_in_central_J20170111-6807-jkj07j.pdf","download_url":"https://www.academia.edu/attachments/51300464/download_file","bulk_download_file_name":"Holocene_glacier_variations_in_central_J.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300464/Holocene_glacier_variations_in_central_J20170111-6807-jkj07j-libre.pdf?1484140093=\u0026response-content-disposition=attachment%3B+filename%3DHolocene_glacier_variations_in_central_J.pdf\u0026Expires=1743853388\u0026Signature=V0Qcjj4sADzukWqvWwVpgU0HOOQpiEuOmJ~YrO4BF26SJ95YG0FjnzOrWJ8hx1LVWKlxncH0JxIdmi6~HXgajg2UIWxZEDxEkr8TLgOrwdV2vPihDvVPUF~2MM-DrMke8ipJqqKSLd8BJG39712LaMozts9JWSOLSHtEtYW6fBC8giU-~8I~kCwORItSHEzsGrbFEUYK5xzVDczF5A~I47mOjRASdpZ6-IAH8uFVRB2~WrKyG5bp2wZJswKY4NdWmGECvK8QqUH4B7tEPxI1LhM9iW1OaeqN-T4OH~YFkRPcukFyAsBzU2VtdzcD9wH3QHuZ~XOcOh9VMso~nZ5wtg__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":13839,"name":"Temporal Resolution","url":"https://www.academia.edu/Documents/in/Temporal_Resolution"},{"id":79294,"name":"Quaternary Science","url":"https://www.academia.edu/Documents/in/Quaternary_Science"},{"id":93755,"name":"History and archaeology","url":"https://www.academia.edu/Documents/in/History_and_archaeology"},{"id":149117,"name":"Magnetic Susceptibility","url":"https://www.academia.edu/Documents/in/Magnetic_Susceptibility"},{"id":150013,"name":"Late Holocene","url":"https://www.academia.edu/Documents/in/Late_Holocene"},{"id":167123,"name":"Loss on Ignition","url":"https://www.academia.edu/Documents/in/Loss_on_Ignition"},{"id":182364,"name":"Little Ice Age","url":"https://www.academia.edu/Documents/in/Little_Ice_Age"},{"id":186099,"name":"Grain size","url":"https://www.academia.edu/Documents/in/Grain_size"},{"id":338205,"name":"Early Holocene","url":"https://www.academia.edu/Documents/in/Early_Holocene"},{"id":373417,"name":"Quaternary Science Reviews","url":"https://www.academia.edu/Documents/in/Quaternary_Science_Reviews"},{"id":630941,"name":"Calcium Carbonate","url":"https://www.academia.edu/Documents/in/Calcium_Carbonate"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874024-figures'); } }); </script> </div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="3302982" id="papers"><div class="js-work-strip profile--work_container" data-work-id="1360476"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/1360476/Holocene_glaciation_and_climate_evolution_of_Baffin_Island_Arctic_Canada"><img alt="Research paper thumbnail of Holocene glaciation and climate evolution of Baffin Island, Arctic Canada" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Holocene glaciation and climate evolution of Baffin Island, Arctic Canada</div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://uib.academia.edu/AtleNesje">Atle Nesje</a> and <a class="" data-click-track="profile-work-strip-authors" href="https://indiana.academia.edu/PeterSauer">Peter E Sauer</a></span></div><div class="wp-workCard_item"><span>Quaternary Science …</span><span>, Jan 1, 2005</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Lake sediment cores and cosmogenic exposure (CE) dates constrain the pattern of deglaciation and ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Lake sediment cores and cosmogenic exposure (CE) dates constrain the pattern of deglaciation and evolution of climate across Baffin Island since the last glacial maximum (LGM). CE dating of erratics demonstrates that the northeastern coastal lowlands became ice-free ca.14ka as the Laurentide Ice Sheet (LIS) receded from its LGM margin on the continental shelf. Coastal lakes in southeastern Baffin Island</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="1360476"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="1360476"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 1360476; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=1360476]").text(description); $(".js-view-count[data-work-id=1360476]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 1360476; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='1360476']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=1360476]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":1360476,"title":"Holocene glaciation and climate evolution of Baffin Island, Arctic Canada","translated_title":"","metadata":{"abstract":"Lake sediment cores and cosmogenic exposure (CE) dates constrain the pattern of deglaciation and evolution of climate across Baffin Island since the last glacial maximum (LGM). 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-1360476-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874042"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874042/Geometry_thickness_and_isostatic_loading_of_the_late_weichselian_scandinavian_ice_sheet"><img alt="Research paper thumbnail of Geometry, thickness and isostatic loading of the late weichselian scandinavian ice sheet" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Geometry, thickness and isostatic loading of the late weichselian scandinavian ice sheet</div><div class="wp-workCard_item"><span>Norsk Geologisk Tidsskrift</span><span>, 1992</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874042"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874042"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874042; 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874042-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874041"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874041/Quantification_of_late_Cenozoic_erosion_and_denudation_in_the_Sognefjord_drainage_basin_western_Norway"><img alt="Research paper thumbnail of Quantification of late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Quantification of late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway</div><div class="wp-workCard_item"><span>Norsk Geogr Tidsskr Nor J Geo</span><span>, 1994</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">ABSTRACT The total late Cenozoic erosion and denudation in the Sognefjord drainage basin, western...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">ABSTRACT The total late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway, has been calculated to about 5400 km3 by subtracting the present topography from a reconstructed preglacial (paléic) surface. This volume corresponds to a mean erosion and denudation of 440 m in the Sognefjord drainage basin. The total volume of subaerial denudation and fluvial activity amounts to about 400 km3. The remaining volume of about 5000 km3 yields a mean glacial erosion of about 400 m in the Sognefjord drainage basin. Assuming glacial erosion in a period of 1 million years during the past 2.57 million years, the average rate of glacial erosion in the Sognefjord drainage basin was about 40cm 1000 yr-1 (0.4mm yr-1).</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874041"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874041"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874041; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874041]").text(description); $(".js-view-count[data-work-id=30874041]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874041; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874041']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=30874041]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874041,"title":"Quantification of late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway","translated_title":"","metadata":{"abstract":"ABSTRACT The total late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway, has been calculated to about 5400 km3 by subtracting the present topography from a reconstructed preglacial (paléic) surface. This volume corresponds to a mean erosion and denudation of 440 m in the Sognefjord drainage basin. The total volume of subaerial denudation and fluvial activity amounts to about 400 km3. The remaining volume of about 5000 km3 yields a mean glacial erosion of about 400 m in the Sognefjord drainage basin. Assuming glacial erosion in a period of 1 million years during the past 2.57 million years, the average rate of glacial erosion in the Sognefjord drainage basin was about 40cm 1000 yr-1 (0.4mm yr-1).","publication_date":{"day":null,"month":null,"year":1994,"errors":{}},"publication_name":"Norsk Geogr Tidsskr Nor J Geo"},"translated_abstract":"ABSTRACT The total late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway, has been calculated to about 5400 km3 by subtracting the present topography from a reconstructed preglacial (paléic) surface. This volume corresponds to a mean erosion and denudation of 440 m in the Sognefjord drainage basin. The total volume of subaerial denudation and fluvial activity amounts to about 400 km3. The remaining volume of about 5000 km3 yields a mean glacial erosion of about 400 m in the Sognefjord drainage basin. Assuming glacial erosion in a period of 1 million years during the past 2.57 million years, the average rate of glacial erosion in the Sognefjord drainage basin was about 40cm 1000 yr-1 (0.4mm yr-1).","internal_url":"https://www.academia.edu/30874041/Quantification_of_late_Cenozoic_erosion_and_denudation_in_the_Sognefjord_drainage_basin_western_Norway","translated_internal_url":"","created_at":"2017-01-11T05:01:33.864-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Quantification_of_late_Cenozoic_erosion_and_denudation_in_the_Sognefjord_drainage_basin_western_Norway","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"ABSTRACT The total late Cenozoic erosion and denudation in the Sognefjord drainage basin, western Norway, has been calculated to about 5400 km3 by subtracting the present topography from a reconstructed preglacial (paléic) surface. This volume corresponds to a mean erosion and denudation of 440 m in the Sognefjord drainage basin. The total volume of subaerial denudation and fluvial activity amounts to about 400 km3. The remaining volume of about 5000 km3 yields a mean glacial erosion of about 400 m in the Sognefjord drainage basin. Assuming glacial erosion in a period of 1 million years during the past 2.57 million years, the average rate of glacial erosion in the Sognefjord drainage basin was about 40cm 1000 yr-1 (0.4mm yr-1).","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[],"research_interests":[{"id":262,"name":"Human Geography","url":"https://www.academia.edu/Documents/in/Human_Geography"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874041-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874040"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/30874040/Glacial_landforms_and_Quaternary_landscape_development_in_Norway"><img alt="Research paper thumbnail of Glacial landforms and Quaternary landscape development in Norway" class="work-thumbnail" src="https://attachments.academia-assets.com/51300480/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/30874040/Glacial_landforms_and_Quaternary_landscape_development_in_Norway">Glacial landforms and Quaternary landscape development in Norway</a></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The Norwegian landscape is a function of geological processes working over very long time spans, ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The Norwegian landscape is a function of geological processes working over very long time spans, and first order structures might for example be traced to the ancient denudational processes, the Caledonian orogeny or break-up of the North Atlantic. However, a large portion of large-, intermediate-, and small-scale landforms in Norway owe their existence to Quaternary glaciations or periglacial processes. The Quaternary time period (the last c. 3 million years), is characterised by cool and variable climate with temperatures oscillating between relative mildness to frigid ice-age conditions. A wide spectrum of climate-driven geomorphological processes has thus been acting in Norway, but the numerous glaciations have had the most profound effect with the production of large U-shaped valleys, fjords and Alpine relief. On the other hand, interior and upland areas in Norway seem to be largely unaffected by glacial erosion and exhibit a possibly pre-Quaternary landscape with only some periglacial influence. The ice sheets in Scandinavia thus have redistributed rock mass and sediments in the landscape with the largest glaciogenic deposits being found on the continental shelf. Large Quaternary deposits and valley fills can also be found onshore and these are now valuable resources for aggregates, ground water and agriculture. Important Quaternary processes have also been acting along the Norwegian coast with denudation of the famous strandflat, where the formation processes are not fully understood. The isostatic depression of crust under the vast ice sheets have also lead to important consequences, with thick deposits of potentially unstable, fine-grained glaciomarine sediments in quite large areas of Norway. It is thus clear that much of Norway's beauty but also geohazard problems can be explained with the actions of Quaternary geomorphological processes.</span></div><div class="wp-workCard_item"><div class="carousel-container carousel-container--sm" id="profile-work-30874040-figures"><div class="prev-slide-container js-prev-button-container"><button aria-label="Previous" class="carousel-navigation-button js-profile-work-30874040-figures-prev"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_back_ios</span></button></div><div class="slides-container js-slides-container"><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375406/figure-1-first-order-glacial-erosion-landforms-are-centred"><img alt="Figure 1. First-order glacial erosion landforms are centred around the Scandinavian mountain chain with fords on the Norwegian coast and deep piedmont lakes east of the mountains " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_001.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375407/figure-2-relict-nonglacial-surfaces-east-of-the-lyngen-fjord"><img alt="Figure 2. Relict nonglacial surfaces east of the Lyngen fjord in Troms. Note that all mountains reach essentially the same altitude and the very flat appearance of the surfaces. These surfaces have probably been connected into a flat, undulating landscape which was uplifted and eroded through fluvial and glacial processes in the Neogene. Total relief in the area, including the ford, is on the order of 2 km. It is evident that glacial erosion has altered the preglacial landscape profoundly in many areas but conversely it also seems likely that pre-Quaternary topography has conditioned glacial erosion. Pre-Quaternary fluvial valleys probably focused glacier ice flow early on in the Quaternary glacial history, thus creating a positive feedback where subsequent ice flow continued to deepen these valleys. It follows, which a large body of geomorphological literature also shows, that Quaternary glaciations have eroded the landscape selectively (e.g., Sugden 1978, Nesje and Whillans 1994, Lidmar-Bergstrém et al. 2000, Li et al. 2005, Fjellanger et al. 2006, Staiger et al. 2005, Phillips et al. 2006), creating mountainous areas with deeply incised troughs and virtually nonaffected uplands. These noneroded uplands are henceforth called relict nonglacial " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_002.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375408/figure-3-was-able-to-create-features-similar-to-both"><img alt="was able to create features similar to both crescentic fractures and gouges. Up-ice concave and convex features were shown to be conditioned by the effective pressure applied by the ball bearing during these experiments, where up-ice concave features preferably formed when a high level of pressure was applied (Smith 1984). Good examples of striae, crescentic fractures and gouges can e.g., be found in the coastal landscape of southern Norway and in front of contemporary glaciers. Roches moutonées and rock drumlins are bedrock cnolls that have been polished by glacial abrasion. Depending yn bedrock joints and grains these landforms often become he glacier has evacuated pre-Quaternary) topogra ‘longated in the ice-flow direction and are thus excellent ndicators of former ice flow. Roches moutonées differ from ‘ock drumlins in that they have a plucked lee-side slope, where parts of the bedrock knoll, probably hrough freeze-on processes. It is debated whether roches noutonées and rock drumlins are governed by a pre-existing phy, perhaps akin to a stripped etch urface or if they are primarily formed by glacial abrasion Lindstr6m 1988, Johansson et al. 2001). Many areas in outhern Norway exhibit beautiful Roches moutonées and rock rumlins; this is probably due to rapid ice movement in the ‘un-up zone for the Norwegian channel ice stream (Sejrup et U. 2000, 2003). knolls that have been polished by glacial abrasion. Depending " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_003.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375409/figure-4-shaped-valley-with-overdeepened-lake-basin-at-lake"><img alt="Figure 4, U-shaped valley with overdeepened lake basin at lake Loen close to Nordford, western Norway Fjords are essentially glacial troughs cut into bedrock below today’s sea level and is perhaps the most prominent landscape feature in Norway (Figure 4). Fjords are formed much in the same way as U-shaped valleys although the overdeepening in fjords may be even more pronounced forming sills at the fford mouth (Lysa et al. 2009). It is thought that these sills were formed due to less glacial erosion at the coast where the former ice tongues spread out and became thinner (Aarseth 1997). As with U-shaped valleys, fords often follows fault zones, which may give rise to distinct fjord networks as is evident for example on the Mare coast (Gabrielsen et al. 2002). Fjords are important sinks for interglacial sediments (Aarseth 1997, Lysa et al. 2009). Indeed Aarseth (1997), calculated that about 150 km3 Holocene sediments reside in the main Norwegian fjords. Aarseth (1997) also considered most fjord sediments to be evacuated during main glaciations and, consequently, transported and deposited onto the continental shelf or shelf break. Subglacial channels may be formed by highly pressurised water, which is governed by the hydraulic potential gradient within the glacier. The subglacial water may thus defy gravity and cause subglacial meltwater channels that are at odds with topography or with an irregular longitudinal profile. Subglacial meltwater channels, naturally, require flowing water beneath the ice and thus indicate warm-based ice. Subglacial channels may be formed by highly pressurised " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_004.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375411/figure-6-smaller-glaciofluvial-erosional-landforms-include"><img alt="Smaller glaciofluvial erosional landforms include potholes (Figure 6) and P-forms. These are local features that are thought to represent highly dynamical, subglacial conditions where large volumes of meltwater are involved (Dahl 1965). formed through the catastrophic drainage of the vast “Nedre Glamsjo’ ice dammed lake about 10,300 years ago (Longva and Toresen 1991). " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_005.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375413/figure-7-end-moraines-or-more-generally-ice-marginal"><img alt="End moraines or more generally ice-marginal moraines are formed at the glacier margin by either: 1) glacier dumping of debris, 2) ablation or freeze-out of debris and, 3) glaciotectonic processes including pushing of proglacial sediments. Other pro- cesses might also be involved, such as rockfall or slope processes depositing material at the glacier margin. A vast amount of lit- erature describes the various types of ice-marginal moraines and depositional processes (e.g., Clayton and Moran 1974, Boulton and Eyles 1979, Hambrey and Huddart 1995, Bennet 2001). End moraines are important glacial landforms since they in- dicate a glacier advance or still-stand and are thus diagnostic in reconstructing ice-sheet dynamics and configurations. One orwegian end moraine, the Vassryggen Younger Dryas end moraine southeast of Stavanger, was used by Jens Esmark to support the theory of ice ages already in 1824 (Worsley 2006, Figure 7). Ice-marginal moraines are common in Norway and are commonly found in the proglacial areas of present glaciers. Many of these end moraines were formed during the ‘Little Ice Age’ (maximum at about AD 1750) and subsequent glacier re- treat (Nesje et al. 1991, Mathews 2005, Burki et al. 2009). Also other Holocene end-moraine zones are common (e.g., Nesje and Kvamme 1991, Figure 8) but the most prominent ice-marginal " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_006.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375414/figure-8-the-olfjellet-moraine-in-nordland-of-likely-pre"><img alt="Figure 8. The Olfjellet moraine in Nordland of likely Pre-Boreal age. Note multiple and complex ridges indicating an oscillating ice margin " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_007.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375416/figure-9-rogen-moraine-at-hartkjolen-in-nord-trondelag"><img alt="Figure 9. Rogen moraine at Hartkjolen in Nord-Trondelag. " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_008.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375418/figure-10-drumlins-on-lista-in-south-norway-shown-in-shaded"><img alt="Figure 10. Drumlins on Lista in South Norway shown in a shaded relief map produced through high-resolution LiDAR digital-elevation data. The drumlins show ice flow from ENE towards the Skagerrak ice stream. " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_009.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375420/figure-10-terrain-such-as-in-jotunheimen-al-hattestrand"><img alt="terrain such as in Jotunheimen. al. 1989, Hattestrand 1997). Based on extensive mapping o ribbed moraines Kleman and Hattestrand (1999) argued that ribbed moraine forms at the transition between cold-based ice and warm-based ice, which is also indicated by Sollid and Sorbe (1994). Ribbed moraine might thus be a good indication of areas beneath an ice sheet where basal temperatures have been low. Extensive areas of ribbed moraine may be found in north- ernmost and eastern Norway (Sollid and Torp 1984, Sollid and Serbel 1994) and many smaller areas can be found in elevated terrain such as in Jotunheimen. " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_010.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375422/figure-11-glacial-striae-reported-by-vorren-and-sollid-and"><img alt="Glacial striae reported by Vorren (1977, 1979) and Sollid and Torp (1984) in South Norway are perhaps the only likely Landforms from the Early and Middle Weichselian (marine isotope stages 5—3) are rare, although several localities from many parts of Norway with Early to Middle Weichselian sediments have been reported (overviews by Mangerud 2004, Mangerud et al. 2011, Olsen et al. this volume). Much of the landform record from these stages has probably been obliterated in Norway by subsequent glacial stages, although widespread glacial-landform systems of Early Weichselian age have been reported from Sweden and Finland (e.g., Lagerback 1998, Hirvas 1991, Kleman 1992, Hattestrand 1998, Fredin and Hattestrand 2002). " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_011.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375424/figure-12-in-interior-areas-in-southeast-norway-there-are"><img alt="In interior areas in southeast Norway there are numerous sets of end moraines, drumlins, Rogen moraine and glacial meltwater channels that likely predate the last glacial maximum (Sollid and Sorbel 1994, Fredin 2004). Nice examples of supposedly pre-LGM meltwater channels and marginal moraines are for example found on and around the Stwlen mountains close to lake Femunden. This general supposition is based on the observation that these landforms are generally incompatible with known LGM and deglaciation ice-flow patterns in the area and considerations of the thermal regime in the ice (Sollid and Sorbel 1994, Fredin 2004). " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_012.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375426/figure-14-shaded-relief-in-combined-bathymetric-and"><img alt="Figure 14. Shaded relief in a combined bathymetric and topographic dataset show- ing the floor of Tafjord. Note the very large submarine rock-avalanche deposits in the fjord. 11). Because the main ice divide in South Norway was situated south of the water divide, large ice-dammed lakes formed, at least partly subglacially—sublaterally, during the deglaciation leading to deposition of ice-dammed lake deposits. When these lakes drained, extensive meltwater erosional landforms were formed together with erosional marks from floating icebergs (Longva and Thoresen 1991). to deposition of ice-dammed lake deposits. When these lakes " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_013.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375428/figure-18-shorelines-are-usually-erosional-landforms"><img alt="Shorelines are usually erosional landforms indicating wave action for a prolonged time period, and are thus indicative of a sustained sea-level stand. On the Norwegian coast, shorelines are common and the most pronounced shorelines typically reflect the highest sea-level stand following the deglaciation, the Younger Dryas ‘main line’, or the Tapes transgression shoreline at around 6300 BP (cf., Andersen 1968, Svendsen and Mangerud 1987, Sorensen et al. 1987, Reite et al. 1999, Romundset et al. 2011). Shorelines may also be formed at the shores of glacial lakes and perched shorelines may be found in abandoned glacial-lake basins. Somewhat related to shorelines are coastal caves, which are also created by coastal erosion (Figure 18). They typically form where a lithological weakness zone in coastal cliffs coincides in altitude with a prolonged sea-level stand, thus allowing wave erosion to act on the weakness zone. Coastal caves are found, e.g., on the More coast and probably date to the Eemian high sea-level stand (Larsen and Mangerud 1989). " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_014.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375430/figure-16-landscape-at-ulset-dominated-by-glaciomarine-clays"><img alt="Figure 16. A landscape at Ulset dominated by glaciomarine clays with significant quick-clay slide scars. " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_015.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375432/figure-16-the-strandflat-is-flat-bedrock-platform-along-most"><img alt="The strandflat is a flat bedrock platform along most of the Norwegian west coast, which extends both above and below Norwegian west coast, which extends both above and below " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_016.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375434/figure-17-gravitational-processes-by-structural-geology"><img alt="Gravitational processes by structural geology (bedrock competence and structure) and the " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_017.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375436/figure-20-photograph-of-potential-rock-avalanche-on"><img alt="Figure 20. Photograph of a potential rock avalanche on Nornesfellet, threatening to fall into the Lyngen fjord and thus jeopardising several communities in the area. There are several similar sites in the area. All are situated on relatively steep glacial trough walls in a zone of high seismic activity (Iain Henderson, pers. comm.). " class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_018.jpg" /></a></figure><figure class="figure-slide-container"><a href="https://www.academia.edu/figures/39375438/figure-19-glacial-landforms-and-quaternary-landscape"><img alt="" class="figure-slide-image" src="https://figures.academia-assets.com/51300480/figure_019.jpg" /></a></figure></div><div class="next-slide-container js-next-button-container"><button aria-label="Next" class="carousel-navigation-button js-profile-work-30874040-figures-next"><span class="material-symbols-outlined" style="font-size: 24px" translate="no">arrow_forward_ios</span></button></div></div></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="3eedc86c7b187333bbaad19f09f428ee" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":51300480,"asset_id":30874040,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/51300480/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874040"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874040"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874040; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874040]").text(description); $(".js-view-count[data-work-id=30874040]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874040; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874040']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "3eedc86c7b187333bbaad19f09f428ee" } } $('.js-work-strip[data-work-id=30874040]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874040,"title":"Glacial landforms and Quaternary landscape development in Norway","translated_title":"","metadata":{"ai_title_tag":"Quaternary Glacial Processes Shaping Norway's Landscape","grobid_abstract":"The Norwegian landscape is a function of geological processes working over very long time spans, and first order structures might for example be traced to the ancient denudational processes, the Caledonian orogeny or break-up of the North Atlantic. However, a large portion of large-, intermediate-, and small-scale landforms in Norway owe their existence to Quaternary glaciations or periglacial processes. The Quaternary time period (the last c. 3 million years), is characterised by cool and variable climate with temperatures oscillating between relative mildness to frigid ice-age conditions. A wide spectrum of climate-driven geomorphological processes has thus been acting in Norway, but the numerous glaciations have had the most profound effect with the production of large U-shaped valleys, fjords and Alpine relief. On the other hand, interior and upland areas in Norway seem to be largely unaffected by glacial erosion and exhibit a possibly pre-Quaternary landscape with only some periglacial influence. The ice sheets in Scandinavia thus have redistributed rock mass and sediments in the landscape with the largest glaciogenic deposits being found on the continental shelf. Large Quaternary deposits and valley fills can also be found onshore and these are now valuable resources for aggregates, ground water and agriculture. Important Quaternary processes have also been acting along the Norwegian coast with denudation of the famous strandflat, where the formation processes are not fully understood. The isostatic depression of crust under the vast ice sheets have also lead to important consequences, with thick deposits of potentially unstable, fine-grained glaciomarine sediments in quite large areas of Norway. It is thus clear that much of Norway's beauty but also geohazard problems can be explained with the actions of Quaternary geomorphological processes.","publication_date":{"day":1,"month":6,"year":2013,"errors":{}},"grobid_abstract_attachment_id":51300480},"translated_abstract":null,"internal_url":"https://www.academia.edu/30874040/Glacial_landforms_and_Quaternary_landscape_development_in_Norway","translated_internal_url":"","created_at":"2017-01-11T05:01:33.459-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":51300480,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300480/thumbnails/1.jpg","file_name":"Glacial_landforms_and_Quaternary_landsca20170111-6810-1gmlzqp.pdf","download_url":"https://www.academia.edu/attachments/51300480/download_file","bulk_download_file_name":"Glacial_landforms_and_Quaternary_landsca.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300480/Glacial_landforms_and_Quaternary_landsca20170111-6810-1gmlzqp-libre.pdf?1484140267=\u0026response-content-disposition=attachment%3B+filename%3DGlacial_landforms_and_Quaternary_landsca.pdf\u0026Expires=1743853385\u0026Signature=P3M7srlDghzgIrV3P15aF6V3o2ABJ46TPV538WxUhxFKvcN-8GZ-Ztdq96TN4g7~YeKSpunWdR-ayRAiHT9TNypsIAlV7TUwa44dMPwUL3u7jg97sayn5Dnp-tmqZ2pRbZs0k7OFP~hp40FTbujFaKl2FW51IL0VUpeDc-ResiEojSb9aAJ0Pfvn6m5K6ISASH9E1OboA27~2YfZq5LY~8IersQH~4w7cSt5cXyDBONWQzxXxNQUIgmOtx8wpqRkA8~FOHinsbU0xG6vPvmtELzLD~A2qmiRAXYjrlzO-zXSb~TMYsnNkC~4O96tg9PxZ-07qmlpZJTGYXkyBxpU6Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Glacial_landforms_and_Quaternary_landscape_development_in_Norway","translated_slug":"","page_count":23,"language":"en","content_type":"Work","summary":"The Norwegian landscape is a function of geological processes working over very long time spans, and first order structures might for example be traced to the ancient denudational processes, the Caledonian orogeny or break-up of the North Atlantic. However, a large portion of large-, intermediate-, and small-scale landforms in Norway owe their existence to Quaternary glaciations or periglacial processes. The Quaternary time period (the last c. 3 million years), is characterised by cool and variable climate with temperatures oscillating between relative mildness to frigid ice-age conditions. A wide spectrum of climate-driven geomorphological processes has thus been acting in Norway, but the numerous glaciations have had the most profound effect with the production of large U-shaped valleys, fjords and Alpine relief. On the other hand, interior and upland areas in Norway seem to be largely unaffected by glacial erosion and exhibit a possibly pre-Quaternary landscape with only some periglacial influence. The ice sheets in Scandinavia thus have redistributed rock mass and sediments in the landscape with the largest glaciogenic deposits being found on the continental shelf. Large Quaternary deposits and valley fills can also be found onshore and these are now valuable resources for aggregates, ground water and agriculture. Important Quaternary processes have also been acting along the Norwegian coast with denudation of the famous strandflat, where the formation processes are not fully understood. The isostatic depression of crust under the vast ice sheets have also lead to important consequences, with thick deposits of potentially unstable, fine-grained glaciomarine sediments in quite large areas of Norway. It is thus clear that much of Norway's beauty but also geohazard problems can be explained with the actions of Quaternary geomorphological processes.","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[{"id":51300480,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300480/thumbnails/1.jpg","file_name":"Glacial_landforms_and_Quaternary_landsca20170111-6810-1gmlzqp.pdf","download_url":"https://www.academia.edu/attachments/51300480/download_file","bulk_download_file_name":"Glacial_landforms_and_Quaternary_landsca.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300480/Glacial_landforms_and_Quaternary_landsca20170111-6810-1gmlzqp-libre.pdf?1484140267=\u0026response-content-disposition=attachment%3B+filename%3DGlacial_landforms_and_Quaternary_landsca.pdf\u0026Expires=1743853385\u0026Signature=P3M7srlDghzgIrV3P15aF6V3o2ABJ46TPV538WxUhxFKvcN-8GZ-Ztdq96TN4g7~YeKSpunWdR-ayRAiHT9TNypsIAlV7TUwa44dMPwUL3u7jg97sayn5Dnp-tmqZ2pRbZs0k7OFP~hp40FTbujFaKl2FW51IL0VUpeDc-ResiEojSb9aAJ0Pfvn6m5K6ISASH9E1OboA27~2YfZq5LY~8IersQH~4w7cSt5cXyDBONWQzxXxNQUIgmOtx8wpqRkA8~FOHinsbU0xG6vPvmtELzLD~A2qmiRAXYjrlzO-zXSb~TMYsnNkC~4O96tg9PxZ-07qmlpZJTGYXkyBxpU6Q__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874039-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874038"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874038/Nordic_seas_climate_variability_over_the_past_2_millennia_a_tropical_link"><img alt="Research paper thumbnail of Nordic seas climate variability over the past 2 millennia - a tropical link" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Nordic seas climate variability over the past 2 millennia - a tropical link</div><div class="wp-workCard_item"><span>Egs Agu Eug Joint Assembly</span><span>, Apr 1, 2003</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">High resolution records of mean annual and summer temperatures over the past 2 millennia have bee...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">High resolution records of mean annual and summer temperatures over the past 2 millennia have been developed for the Nordic Seas and adjacent land areas with decadal resolution. A new high quality age model for these records has been developed using a novel tree-ring correlation. The data show a very strong land-ocean coherence. Correlation to instrumental time series is also strong. A remarkable correspondance with proxy records of the nortward extent of the ITZC is apparent in the data, based on correlations to a rainfall/runoff proxy from Cariaco Basin off Venezuela. Further comparisons with long time series of North Atlantic indices based on instrumental data and proxy records are underway and will be reported. The strong tropical linkage is also noticeable in the instrumental time series, indicating possible tropical influence on decadal to century climate changes in the high latitude North Atlantic.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874038"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874038"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874038; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874038]").text(description); $(".js-view-count[data-work-id=30874038]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874038; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874038']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=30874038]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874038,"title":"Nordic seas climate variability over the past 2 millennia - a tropical link","translated_title":"","metadata":{"abstract":"High resolution records of mean annual and summer temperatures over the past 2 millennia have been developed for the Nordic Seas and adjacent land areas with decadal resolution. A new high quality age model for these records has been developed using a novel tree-ring correlation. The data show a very strong land-ocean coherence. Correlation to instrumental time series is also strong. A remarkable correspondance with proxy records of the nortward extent of the ITZC is apparent in the data, based on correlations to a rainfall/runoff proxy from Cariaco Basin off Venezuela. Further comparisons with long time series of North Atlantic indices based on instrumental data and proxy records are underway and will be reported. The strong tropical linkage is also noticeable in the instrumental time series, indicating possible tropical influence on decadal to century climate changes in the high latitude North Atlantic.","publication_date":{"day":1,"month":4,"year":2003,"errors":{}},"publication_name":"Egs Agu Eug Joint Assembly"},"translated_abstract":"High resolution records of mean annual and summer temperatures over the past 2 millennia have been developed for the Nordic Seas and adjacent land areas with decadal resolution. A new high quality age model for these records has been developed using a novel tree-ring correlation. The data show a very strong land-ocean coherence. Correlation to instrumental time series is also strong. A remarkable correspondance with proxy records of the nortward extent of the ITZC is apparent in the data, based on correlations to a rainfall/runoff proxy from Cariaco Basin off Venezuela. Further comparisons with long time series of North Atlantic indices based on instrumental data and proxy records are underway and will be reported. The strong tropical linkage is also noticeable in the instrumental time series, indicating possible tropical influence on decadal to century climate changes in the high latitude North Atlantic.","internal_url":"https://www.academia.edu/30874038/Nordic_seas_climate_variability_over_the_past_2_millennia_a_tropical_link","translated_internal_url":"","created_at":"2017-01-11T05:01:32.004-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Nordic_seas_climate_variability_over_the_past_2_millennia_a_tropical_link","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"High resolution records of mean annual and summer temperatures over the past 2 millennia have been developed for the Nordic Seas and adjacent land areas with decadal resolution. A new high quality age model for these records has been developed using a novel tree-ring correlation. The data show a very strong land-ocean coherence. Correlation to instrumental time series is also strong. A remarkable correspondance with proxy records of the nortward extent of the ITZC is apparent in the data, based on correlations to a rainfall/runoff proxy from Cariaco Basin off Venezuela. Further comparisons with long time series of North Atlantic indices based on instrumental data and proxy records are underway and will be reported. The strong tropical linkage is also noticeable in the instrumental time series, indicating possible tropical influence on decadal to century climate changes in the high latitude North Atlantic.","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[],"research_interests":[{"id":1512,"name":"Climate Change","url":"https://www.academia.edu/Documents/in/Climate_Change"},{"id":4456,"name":"Time Series","url":"https://www.academia.edu/Documents/in/Time_Series"},{"id":4753,"name":"Climate variability","url":"https://www.academia.edu/Documents/in/Climate_variability"},{"id":82675,"name":"North Atlantic","url":"https://www.academia.edu/Documents/in/North_Atlantic"},{"id":309086,"name":"High Resolution","url":"https://www.academia.edu/Documents/in/High_Resolution"},{"id":630543,"name":"Tree Ring","url":"https://www.academia.edu/Documents/in/Tree_Ring"}],"urls":[{"id":7880223,"url":"http://adsabs.harvard.edu/abs/2003EAEJA....13421J"}]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874038-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="25981257"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/25981257/Holocene_glacier_fluctuations"><img alt="Research paper thumbnail of Holocene glacier fluctuations" class="work-thumbnail" src="https://attachments.academia-assets.com/46331647/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/25981257/Holocene_glacier_fluctuations">Holocene glacier fluctuations</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/VJomelli">V. Jomelli</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/GregoryWiles">Gregory Wiles</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://ncsu.academia.edu/LewisOwen">Lewis A Owen</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://uib.academia.edu/AtleNesje">Atle Nesje</a>, and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/HodgsonDominic">Dominic Hodgson</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">A global overview of glacier advances and retreats (grouped by regions and by millennia) for the ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">A global overview of glacier advances and retreats (grouped by regions and by millennia) for the Holocene is compiled from previous studies. The reconstructions of glacier fluctuations are based on 1) mapping and dating moraines defined by 14 C, TCN, OSL, lichenometry and tree rings (discontinuous records/time series), and 2) sediments from proglacial lakes and speleothems (continuous records/ time series). Using 189 continuous and discontinuous time series, the long-term trends and centennial fluctuations of glaciers were compared to trends in the recession of Northern and mountain tree lines, and with orbital, solar and volcanic studies to examine the likely forcing factors that drove the changes recorded. A general trend of increasing glacier size from the earlyemid Holocene, to the late</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="4b9c23e02878a0de47d709dce89d193c" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":46331647,"asset_id":25981257,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/46331647/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="25981257"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="25981257"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 25981257; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=25981257]").text(description); $(".js-view-count[data-work-id=25981257]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 25981257; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='25981257']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "4b9c23e02878a0de47d709dce89d193c" } } $('.js-work-strip[data-work-id=25981257]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":25981257,"title":"Holocene glacier fluctuations","translated_title":"","metadata":{"abstract":"A global overview of glacier advances and retreats (grouped by regions and by millennia) for the Holocene is compiled from previous studies. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-25981257-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874036"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/30874036/Late_Holocene_glaciers_and_avalanche_activity_in_the_%C3%85lfotbreen_area_western_Norway_evidence_from_a_lacustrine_sedimentary_record"><img alt="Research paper thumbnail of Late Holocene glaciers and avalanche activity in the Ålfotbreen area, western Norway: evidence from a lacustrine sedimentary record" class="work-thumbnail" src="https://attachments.academia-assets.com/51300478/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/30874036/Late_Holocene_glaciers_and_avalanche_activity_in_the_%C3%85lfotbreen_area_western_Norway_evidence_from_a_lacustrine_sedimentary_record">Late Holocene glaciers and avalanche activity in the Ålfotbreen area, western Norway: evidence from a lacustrine sedimentary record</a></div><div class="wp-workCard_item"><span>Norsk Geologisk Tiddsskrift</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d4214eef2cb5b251cf423f8bf574d85e" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":51300478,"asset_id":30874036,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/51300478/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874036"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874036"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874036; 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This study investigates the lacustrine sedimentary record in the Ålfotbreen area of western Norway, focusing on the evidence for glacier dynamics over the Late Holocene. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874036-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874035"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/30874035/Holocene_mean_July_temperature_and_winter_precipitation_in_western_Norway_inferred_from_lake_sediment_proxies"><img alt="Research paper thumbnail of Holocene mean July temperature and winter precipitation in western Norway inferred from lake sediment proxies" class="work-thumbnail" src="https://attachments.academia-assets.com/51300474/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/30874035/Holocene_mean_July_temperature_and_winter_precipitation_in_western_Norway_inferred_from_lake_sediment_proxies">Holocene mean July temperature and winter precipitation in western Norway inferred from lake sediment proxies</a></div><div class="wp-workCard_item"><span>The Holocene</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Reconstructions of mean July temperature (T jul ) and winter precipitation (P w ) for the last 11...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Reconstructions of mean July temperature (T jul ) and winter precipitation (P w ) for the last 11/500 years on the Folgefonna peninsula are presented. T jul was reconstructed using pollen Á/climate transfer functions and P w was reconstructed based on the exponential relationship between mean solid winter precipitation and ablation-season temperature at the equilibrium-line altitude (ELA) with a reconstructed former ELA, using T jul as the proxy for ablation-season temperature. The reconstructions from the Folgefonna peninsula suggest that the early Holocene was relatively cool and dry until c. 8000 cal. yr BP, followed by a warm and humid mid-Holocene until c. 4000 cal. yr BP with inferred T jul above 128C and P w reaching as high as 225% of the present day. Subsequent to c. 4000 cal. yr BP a reduction is seen in both inferred T jul and P w with large fluctuations during the last 500 years. In addition, new calculations of P w from two glaciers (Hardangerjøkulen and Jostedalsbreen) in southern Norway are presented. The results show that P w varied in phase at all glaciers, probably as a response to the same climate forcing factor. During the early Holocene a major shift is suggested between winds from the west and the east.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="2b626bfa6982729c2b552c3fddedff48" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":51300474,"asset_id":30874035,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/51300474/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874035"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874035"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874035; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874035]").text(description); $(".js-view-count[data-work-id=30874035]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874035; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874035']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "2b626bfa6982729c2b552c3fddedff48" } } $('.js-work-strip[data-work-id=30874035]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874035,"title":"Holocene mean July temperature and winter precipitation in western Norway inferred from lake sediment proxies","translated_title":"","metadata":{"grobid_abstract":"Reconstructions of mean July temperature (T jul ) and winter precipitation (P w ) for the last 11/500 years on the Folgefonna peninsula are presented. T jul was reconstructed using pollen Á/climate transfer functions and P w was reconstructed based on the exponential relationship between mean solid winter precipitation and ablation-season temperature at the equilibrium-line altitude (ELA) with a reconstructed former ELA, using T jul as the proxy for ablation-season temperature. The reconstructions from the Folgefonna peninsula suggest that the early Holocene was relatively cool and dry until c. 8000 cal. yr BP, followed by a warm and humid mid-Holocene until c. 4000 cal. yr BP with inferred T jul above 128C and P w reaching as high as 225% of the present day. Subsequent to c. 4000 cal. yr BP a reduction is seen in both inferred T jul and P w with large fluctuations during the last 500 years. In addition, new calculations of P w from two glaciers (Hardangerjøkulen and Jostedalsbreen) in southern Norway are presented. The results show that P w varied in phase at all glaciers, probably as a response to the same climate forcing factor. 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T jul was reconstructed using pollen Á/climate transfer functions and P w was reconstructed based on the exponential relationship between mean solid winter precipitation and ablation-season temperature at the equilibrium-line altitude (ELA) with a reconstructed former ELA, using T jul as the proxy for ablation-season temperature. The reconstructions from the Folgefonna peninsula suggest that the early Holocene was relatively cool and dry until c. 8000 cal. yr BP, followed by a warm and humid mid-Holocene until c. 4000 cal. yr BP with inferred T jul above 128C and P w reaching as high as 225% of the present day. Subsequent to c. 4000 cal. yr BP a reduction is seen in both inferred T jul and P w with large fluctuations during the last 500 years. In addition, new calculations of P w from two glaciers (Hardangerjøkulen and Jostedalsbreen) in southern Norway are presented. The results show that P w varied in phase at all glaciers, probably as a response to the same climate forcing factor. 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evidence from lake sediments and terrestrial deposits</a></div><div class="wp-workCard_item"><span>Quaternary Science Reviews</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The valleys surroundingthe Jostedalsbreen ice cap were deglaciated during the latter half of the ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The valleys surroundingthe Jostedalsbreen ice cap were deglaciated during the latter half of the Preboreal Chronozone. At the end of the Preboreal Chronozone, however, a glacier readvance occurred. Terminal moraines were deposited by outlet valley glaciers from the Jostedalsbreen Plateau up to 1 km beyond Little Ice A~ge moraines. Inferred from the altitude of lateral moraines formed during this readvance and calculations of the equilibrium-line altitude (ELA) depression based on an accumulation area ratio (AAR) of 0.6, the average depression of the ELA was 325 +75/-115 m below the present. By assuming a similar precipitation pattern as at present, this suggests a mean temperature decline of about 2°C. Palynological investigations from Sygneskardet, Sunndalen, indicate that climate like the present was achieved just after 9000 BP. The Holocene climatic optimum occurred during the Atlantic Chronozone, with elm (Ulmus) stands growing at the present birch (Betula) forest limit in Sunndalen and pine (Pinus) growing at Styggevatnet to an altitude of at least 1160 m. Durin[g this period the mean summer temperature is estimated to have been at least 2.7 and 1.8°C warmer than at present, with and wtthout the local climatic effect of Jostedalsbreen, respectively. An inferred rise of the ELA of about 400 m from the present altitude suggests that possibly no glaciers existed on the Jostedalsbreen Plateau during the Holocene climatic optimum. Vegetational chan~es as deduced from palynological studies, lowered tree limits and increased resedimentation in peat bogs indicate general climatic deterioration since the Late Atlantic Chronozone.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="1dda190660f62119501b7ffa70db0dbc" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":51300471,"asset_id":30874031,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/51300471/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874031"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874031"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874031; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874031]").text(description); $(".js-view-count[data-work-id=30874031]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874031; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874031']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "1dda190660f62119501b7ffa70db0dbc" } } $('.js-work-strip[data-work-id=30874031]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874031,"title":"Holocene glacial and climate history of the Jostedalsbreen region, Western Norway; evidence from lake sediments and terrestrial deposits","translated_title":"","metadata":{"ai_title_tag":"Holocene Climate and Glacial History of Jostedalsbreen","grobid_abstract":"The valleys surroundingthe Jostedalsbreen ice cap were deglaciated during the latter half of the Preboreal Chronozone. At the end of the Preboreal Chronozone, however, a glacier readvance occurred. Terminal moraines were deposited by outlet valley glaciers from the Jostedalsbreen Plateau up to 1 km beyond Little Ice A~ge moraines. Inferred from the altitude of lateral moraines formed during this readvance and calculations of the equilibrium-line altitude (ELA) depression based on an accumulation area ratio (AAR) of 0.6, the average depression of the ELA was 325 +75/-115 m below the present. By assuming a similar precipitation pattern as at present, this suggests a mean temperature decline of about 2°C. Palynological investigations from Sygneskardet, Sunndalen, indicate that climate like the present was achieved just after 9000 BP. The Holocene climatic optimum occurred during the Atlantic Chronozone, with elm (Ulmus) stands growing at the present birch (Betula) forest limit in Sunndalen and pine (Pinus) growing at Styggevatnet to an altitude of at least 1160 m. 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Vegetational chan~es as deduced from palynological studies, lowered tree limits and increased resedimentation in peat bogs indicate general climatic deterioration since the Late Atlantic Chronozone.","publication_name":"Quaternary Science Reviews","grobid_abstract_attachment_id":51300471},"translated_abstract":null,"internal_url":"https://www.academia.edu/30874031/Holocene_glacial_and_climate_history_of_the_Jostedalsbreen_region_Western_Norway_evidence_from_lake_sediments_and_terrestrial_deposits","translated_internal_url":"","created_at":"2017-01-11T05:01:28.434-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":51300471,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300471/thumbnails/1.jpg","file_name":"Holocene_glacial_and_climate_history_of_20170111-6810-17x38bn.pdf","download_url":"https://www.academia.edu/attachments/51300471/download_file","bulk_download_file_name":"Holocene_glacial_and_climate_history_of.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300471/Holocene_glacial_and_climate_history_of_20170111-6810-17x38bn-libre.pdf?1484140105=\u0026response-content-disposition=attachment%3B+filename%3DHolocene_glacial_and_climate_history_of.pdf\u0026Expires=1743853387\u0026Signature=e~A880Cqd9dWh9ngMN4ejUu3NLTix3eSHTWo0QKZSIPjcz0kD~noUM-nYL9F9e0bwqU0MArZE39b86Ev-FLsty4ON8r5Ugwu4XhamHbQvfC8RdkbSyPxmR8pk-tsIavYctxNwX2r32MUfFO4rNz1Hhz3eeLSFwRvCN4XWjxy7Rm-d-ebMUg-foAv0cQgHceN~iBNngEOrOoWr4CnIFrPSU35BrbmJcrENFE5iw83zsQ1~UZ8c-g4B0aVToRI-Djku01wC13TmFX-nYqGYfMQQ-d1t6Cg2Tc60cGXTvpgpHHnGNBj67PRzw97qae-TI0nHtZbt7DJtScV0JxVVDdNnw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Holocene_glacial_and_climate_history_of_the_Jostedalsbreen_region_Western_Norway_evidence_from_lake_sediments_and_terrestrial_deposits","translated_slug":"","page_count":29,"language":"en","content_type":"Work","summary":"The valleys surroundingthe Jostedalsbreen ice cap were deglaciated during the latter half of the Preboreal Chronozone. 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Durin[g this period the mean summer temperature is estimated to have been at least 2.7 and 1.8°C warmer than at present, with and wtthout the local climatic effect of Jostedalsbreen, respectively. An inferred rise of the ELA of about 400 m from the present altitude suggests that possibly no glaciers existed on the Jostedalsbreen Plateau during the Holocene climatic optimum. Vegetational chan~es as deduced from palynological studies, lowered tree limits and increased resedimentation in peat bogs indicate general climatic deterioration since the Late Atlantic Chronozone.","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[{"id":51300471,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300471/thumbnails/1.jpg","file_name":"Holocene_glacial_and_climate_history_of_20170111-6810-17x38bn.pdf","download_url":"https://www.academia.edu/attachments/51300471/download_file","bulk_download_file_name":"Holocene_glacial_and_climate_history_of.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300471/Holocene_glacial_and_climate_history_of_20170111-6810-17x38bn-libre.pdf?1484140105=\u0026response-content-disposition=attachment%3B+filename%3DHolocene_glacial_and_climate_history_of.pdf\u0026Expires=1743853387\u0026Signature=e~A880Cqd9dWh9ngMN4ejUu3NLTix3eSHTWo0QKZSIPjcz0kD~noUM-nYL9F9e0bwqU0MArZE39b86Ev-FLsty4ON8r5Ugwu4XhamHbQvfC8RdkbSyPxmR8pk-tsIavYctxNwX2r32MUfFO4rNz1Hhz3eeLSFwRvCN4XWjxy7Rm-d-ebMUg-foAv0cQgHceN~iBNngEOrOoWr4CnIFrPSU35BrbmJcrENFE5iw83zsQ1~UZ8c-g4B0aVToRI-Djku01wC13TmFX-nYqGYfMQQ-d1t6Cg2Tc60cGXTvpgpHHnGNBj67PRzw97qae-TI0nHtZbt7DJtScV0JxVVDdNnw__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[{"id":400,"name":"Earth Sciences","url":"https://www.academia.edu/Documents/in/Earth_Sciences"},{"id":93755,"name":"History and archaeology","url":"https://www.academia.edu/Documents/in/History_and_archaeology"},{"id":373417,"name":"Quaternary Science Reviews","url":"https://www.academia.edu/Documents/in/Quaternary_Science_Reviews"}],"urls":[]}, dispatcherData: dispatcherData }); 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874029-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874028"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874028/The_Expression_of_the_8_2_ka_and_Younger_Dryas_Events_in_the_Eastern_Canadian_Arctic"><img alt="Research paper thumbnail of The Expression of the 8.2 ka and Younger Dryas Events in the Eastern Canadian Arctic" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">The Expression of the 8.2 ka and Younger Dryas Events in the Eastern Canadian Arctic</div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The two largest climate coolings following the end of the last glaciation are the Younger Dryas a...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The two largest climate coolings following the end of the last glaciation are the Younger Dryas and the 8.2 ka events. Evidence for these cold excursions is widespread around the North Atlantic and in more distant regions. Both events are well expressed in Greenland ice cores; glacier readvances occurred across much of NW Europe during the Younger Dryas and cold surface waters returned to the North Atlantic, with depressed summer temperatures in eastern North America. The 8.2 ka event has a similar pattern, but the magnitude is substantially lower, with a much shorter duration. However, surprisingly little evidence has been presented for either event from the North Atlantic Arctic. Recently acquired lake sediment records from the Eastern Canadian Arctic contain evidence for both excursions. The 8.2 ka event is recorded at two sites as a significant glacier readvance of cirque and outlet glaciers of local ice caps at 8.2±0.1 ka. In some non-glacially-dominated lakes, a reduction in primary productivity is apparent at the same time. These records suggest colder summers without a dramatic reduction in precipitation, producing positive mass balances and glacier readvances. For most local glaciers, this was the last significant readvance before they receded behind their Little Ice Age margins. Only a few lakes contain records that extend through the Younger Dryas chron. The best-dated lake record, Donard Lake, extends back to 15 ka. Lacustrine sedimentation is currently dominated by a meltwater from an outlet glacier that terminates a few hundred meters from the lake. The glacier has been within the drainage basin of the lake for the past 5.5 ka, although the contribution of glacial sediment has been larger since about 2.5 ka. Prior to 5.5 ka, there is no evidence of a glacier in the catchment of Donard Lake, suggesting that throughout the entire Neoglacial period, the local glacier has been more advanced than at any time since 15 ka. During the Younger Dryas chron, lacustrine primary productivity was greatly reduced, whether measured as the flux of organic carbon to the lake floor or as the percentage of organic matter in lake sediment. We interpret this change to reflect a substantial reduction in summer temperatures for more than 1 ka. However, this temperature drop was not accompanied by a significant glacier readvance, suggesting precipitation must have been very low. This differs from the 8.2 ka event when precipitation must have remained relatively high. These records indicate that in the Eastern Canadian Arctic, summers during the Younger Dryas were much colder than present, but precipitation was dramatically lower too, so glaciers did not advance, whereas during the briefer, and less severe summer cooling associated with the 8.2 ka event, precipitation was not dramatically reduced and glaciers readvanced.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874028"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874028"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874028; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874028]").text(description); $(".js-view-count[data-work-id=30874028]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874028; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874028']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=30874028]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874028,"title":"The Expression of the 8.2 ka and Younger Dryas Events in the Eastern Canadian Arctic","translated_title":"","metadata":{"abstract":"The two largest climate coolings following the end of the last glaciation are the Younger Dryas and the 8.2 ka events. Evidence for these cold excursions is widespread around the North Atlantic and in more distant regions. Both events are well expressed in Greenland ice cores; glacier readvances occurred across much of NW Europe during the Younger Dryas and cold surface waters returned to the North Atlantic, with depressed summer temperatures in eastern North America. The 8.2 ka event has a similar pattern, but the magnitude is substantially lower, with a much shorter duration. However, surprisingly little evidence has been presented for either event from the North Atlantic Arctic. Recently acquired lake sediment records from the Eastern Canadian Arctic contain evidence for both excursions. The 8.2 ka event is recorded at two sites as a significant glacier readvance of cirque and outlet glaciers of local ice caps at 8.2±0.1 ka. In some non-glacially-dominated lakes, a reduction in primary productivity is apparent at the same time. These records suggest colder summers without a dramatic reduction in precipitation, producing positive mass balances and glacier readvances. For most local glaciers, this was the last significant readvance before they receded behind their Little Ice Age margins. Only a few lakes contain records that extend through the Younger Dryas chron. The best-dated lake record, Donard Lake, extends back to 15 ka. Lacustrine sedimentation is currently dominated by a meltwater from an outlet glacier that terminates a few hundred meters from the lake. The glacier has been within the drainage basin of the lake for the past 5.5 ka, although the contribution of glacial sediment has been larger since about 2.5 ka. Prior to 5.5 ka, there is no evidence of a glacier in the catchment of Donard Lake, suggesting that throughout the entire Neoglacial period, the local glacier has been more advanced than at any time since 15 ka. During the Younger Dryas chron, lacustrine primary productivity was greatly reduced, whether measured as the flux of organic carbon to the lake floor or as the percentage of organic matter in lake sediment. We interpret this change to reflect a substantial reduction in summer temperatures for more than 1 ka. However, this temperature drop was not accompanied by a significant glacier readvance, suggesting precipitation must have been very low. This differs from the 8.2 ka event when precipitation must have remained relatively high. These records indicate that in the Eastern Canadian Arctic, summers during the Younger Dryas were much colder than present, but precipitation was dramatically lower too, so glaciers did not advance, whereas during the briefer, and less severe summer cooling associated with the 8.2 ka event, precipitation was not dramatically reduced and glaciers readvanced."},"translated_abstract":"The two largest climate coolings following the end of the last glaciation are the Younger Dryas and the 8.2 ka events. Evidence for these cold excursions is widespread around the North Atlantic and in more distant regions. Both events are well expressed in Greenland ice cores; glacier readvances occurred across much of NW Europe during the Younger Dryas and cold surface waters returned to the North Atlantic, with depressed summer temperatures in eastern North America. The 8.2 ka event has a similar pattern, but the magnitude is substantially lower, with a much shorter duration. However, surprisingly little evidence has been presented for either event from the North Atlantic Arctic. Recently acquired lake sediment records from the Eastern Canadian Arctic contain evidence for both excursions. The 8.2 ka event is recorded at two sites as a significant glacier readvance of cirque and outlet glaciers of local ice caps at 8.2±0.1 ka. In some non-glacially-dominated lakes, a reduction in primary productivity is apparent at the same time. These records suggest colder summers without a dramatic reduction in precipitation, producing positive mass balances and glacier readvances. For most local glaciers, this was the last significant readvance before they receded behind their Little Ice Age margins. Only a few lakes contain records that extend through the Younger Dryas chron. The best-dated lake record, Donard Lake, extends back to 15 ka. Lacustrine sedimentation is currently dominated by a meltwater from an outlet glacier that terminates a few hundred meters from the lake. The glacier has been within the drainage basin of the lake for the past 5.5 ka, although the contribution of glacial sediment has been larger since about 2.5 ka. Prior to 5.5 ka, there is no evidence of a glacier in the catchment of Donard Lake, suggesting that throughout the entire Neoglacial period, the local glacier has been more advanced than at any time since 15 ka. During the Younger Dryas chron, lacustrine primary productivity was greatly reduced, whether measured as the flux of organic carbon to the lake floor or as the percentage of organic matter in lake sediment. We interpret this change to reflect a substantial reduction in summer temperatures for more than 1 ka. However, this temperature drop was not accompanied by a significant glacier readvance, suggesting precipitation must have been very low. 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These records suggest colder summers without a dramatic reduction in precipitation, producing positive mass balances and glacier readvances. For most local glaciers, this was the last significant readvance before they receded behind their Little Ice Age margins. Only a few lakes contain records that extend through the Younger Dryas chron. The best-dated lake record, Donard Lake, extends back to 15 ka. Lacustrine sedimentation is currently dominated by a meltwater from an outlet glacier that terminates a few hundred meters from the lake. The glacier has been within the drainage basin of the lake for the past 5.5 ka, although the contribution of glacial sediment has been larger since about 2.5 ka. Prior to 5.5 ka, there is no evidence of a glacier in the catchment of Donard Lake, suggesting that throughout the entire Neoglacial period, the local glacier has been more advanced than at any time since 15 ka. During the Younger Dryas chron, lacustrine primary productivity was greatly reduced, whether measured as the flux of organic carbon to the lake floor or as the percentage of organic matter in lake sediment. We interpret this change to reflect a substantial reduction in summer temperatures for more than 1 ka. However, this temperature drop was not accompanied by a significant glacier readvance, suggesting precipitation must have been very low. This differs from the 8.2 ka event when precipitation must have remained relatively high. These records indicate that in the Eastern Canadian Arctic, summers during the Younger Dryas were much colder than present, but precipitation was dramatically lower too, so glaciers did not advance, whereas during the briefer, and less severe summer cooling associated with the 8.2 ka event, precipitation was not dramatically reduced and glaciers readvanced.","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[],"research_interests":[{"id":42073,"name":"North Eastern North America Archaeology","url":"https://www.academia.edu/Documents/in/North_Eastern_North_America_Archaeology"},{"id":82675,"name":"North Atlantic","url":"https://www.academia.edu/Documents/in/North_Atlantic"},{"id":142810,"name":"Surface Water","url":"https://www.academia.edu/Documents/in/Surface_Water"},{"id":152776,"name":"Younger Dryas","url":"https://www.academia.edu/Documents/in/Younger_Dryas"},{"id":182364,"name":"Little Ice Age","url":"https://www.academia.edu/Documents/in/Little_Ice_Age"},{"id":198868,"name":"Ice Cores","url":"https://www.academia.edu/Documents/in/Ice_Cores"},{"id":289852,"name":"Primary Production","url":"https://www.academia.edu/Documents/in/Primary_Production"},{"id":585192,"name":"Organic carbon","url":"https://www.academia.edu/Documents/in/Organic_carbon"},{"id":970387,"name":"Organic Matter","url":"https://www.academia.edu/Documents/in/Organic_Matter"},{"id":1707373,"name":"Mass Balance","url":"https://www.academia.edu/Documents/in/Mass_Balance"},{"id":2196834,"name":"Canadian Arctic","url":"https://www.academia.edu/Documents/in/Canadian_Arctic"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874028-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874027"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874027/Holocene_Changes_in_Atmospherical_Circulation_in_the_North_Atlantic_Region_Evidences_for_Millennial_Scale_coVariability_Between_Ocean_and_Atmosphere_Circulation"><img alt="Research paper thumbnail of Holocene Changes in Atmospherical Circulation in the North Atlantic Region - Evidences for Millennial-Scale coVariability Between Ocean and Atmosphere Circulation" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Holocene Changes in Atmospherical Circulation in the North Atlantic Region - Evidences for Millennial-Scale coVariability Between Ocean and Atmosphere Circulation</div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Whereas a number of records from the marine realm have demonstrated Holocene changes regarded to ...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Whereas a number of records from the marine realm have demonstrated Holocene changes regarded to be related to overturning circulation in the North Atlantic region, independent information of atmospherical variability from the terrestrial realm have proven more elusive to capture in palaeo-records. This is a major concern, as several studies have suggested that atmospherical forcing may be an important factor</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874027"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874027"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874027; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874027]").text(description); $(".js-view-count[data-work-id=30874027]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874027; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874027']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (false){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "-1" } } $('.js-work-strip[data-work-id=30874027]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874027,"title":"Holocene Changes in Atmospherical Circulation in the North Atlantic Region - Evidences for Millennial-Scale coVariability Between Ocean and Atmosphere Circulation","translated_title":"","metadata":{"abstract":"Whereas a number of records from the marine realm have demonstrated Holocene changes regarded to be related to overturning circulation in the North Atlantic region, independent information of atmospherical variability from the terrestrial realm have proven more elusive to capture in palaeo-records. 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This is a major concern, as several studies have suggested that atmospherical forcing may be an important factor","internal_url":"https://www.academia.edu/30874027/Holocene_Changes_in_Atmospherical_Circulation_in_the_North_Atlantic_Region_Evidences_for_Millennial_Scale_coVariability_Between_Ocean_and_Atmosphere_Circulation","translated_internal_url":"","created_at":"2017-01-11T05:01:26.529-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[],"slug":"Holocene_Changes_in_Atmospherical_Circulation_in_the_North_Atlantic_Region_Evidences_for_Millennial_Scale_coVariability_Between_Ocean_and_Atmosphere_Circulation","translated_slug":"","page_count":null,"language":"en","content_type":"Work","summary":"Whereas a number of records from the marine realm have demonstrated Holocene changes regarded to be related to overturning circulation in the North Atlantic region, independent information of atmospherical variability from the terrestrial realm have proven more elusive to capture in palaeo-records. This is a major concern, as several studies have suggested that atmospherical forcing may be an important factor","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[],"research_interests":[{"id":30441,"name":"North Atlantic Ocean","url":"https://www.academia.edu/Documents/in/North_Atlantic_Ocean"},{"id":44265,"name":"North Atlantic Oscillation","url":"https://www.academia.edu/Documents/in/North_Atlantic_Oscillation"},{"id":62729,"name":"Air flow","url":"https://www.academia.edu/Documents/in/Air_flow"},{"id":82675,"name":"North Atlantic","url":"https://www.academia.edu/Documents/in/North_Atlantic"},{"id":113239,"name":"Ocean Circulation","url":"https://www.academia.edu/Documents/in/Ocean_Circulation"},{"id":150013,"name":"Late Holocene","url":"https://www.academia.edu/Documents/in/Late_Holocene"},{"id":236377,"name":"Spatial Distribution","url":"https://www.academia.edu/Documents/in/Spatial_Distribution"},{"id":303826,"name":"Atmospheric Circulation","url":"https://www.academia.edu/Documents/in/Atmospheric_Circulation"},{"id":314103,"name":"Inverse Modeling","url":"https://www.academia.edu/Documents/in/Inverse_Modeling"},{"id":2516014,"name":"temporal variation","url":"https://www.academia.edu/Documents/in/temporal_variation"}],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874027-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874026"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/30874026/Holocene_glacial_and_colluvial_activity_in_Leirungsdalen_eastern_Jotunheimen_south_central_Norway"><img alt="Research paper thumbnail of Holocene glacial and colluvial activity in Leirungsdalen, eastern Jotunheimen, south-central Norway" class="work-thumbnail" src="https://attachments.academia-assets.com/51300462/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/30874026/Holocene_glacial_and_colluvial_activity_in_Leirungsdalen_eastern_Jotunheimen_south_central_Norway">Holocene glacial and colluvial activity in Leirungsdalen, eastern Jotunheimen, south-central Norway</a></div><div class="wp-workCard_item"><span>Norsk Geologisk Tidsskrift</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Two terrestrial sections have been studied in order to reconstruct the Holocene glacial and collu...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Two terrestrial sections have been studied in order to reconstruct the Holocene glacial and colluvial history in Leirungsdalen, eastern Jotunheimen. The interpretation of individual sedimentary units is based on the grain-size distribution and compared with modern analogue samples collected in the respective streams and at sites close to the present glaciers. Stages of enhanced debris flow or glacial activity are recognized as sand and silt layers, respectively, while periods of low colluvial and glacial activity in the catchment are characterised by continuous peat accumulation. Age/depth curves based on radiocarbon dates from the Svarthammarbu and Steinflybekken sections indicate debris flow activity &gt; 7500, 7300-6800,6600-5500, 5800, 5700, 5300-4900,4700, 4500,4300, 2300, 2100-1500, 1300, 700-600 and 500-400 cal. yr BP. The first Holocene glacial signal is detected ca. 5300 cal. yr BP. The frequency of glacial events seems to have increased during the Late Holocene, especially...</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="d5b96cb3db7fcf5a11208098f5d18905" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":51300462,"asset_id":30874026,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/51300462/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="30874026"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="30874026"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 30874026; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=30874026]").text(description); $(".js-view-count[data-work-id=30874026]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 30874026; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='30874026']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "d5b96cb3db7fcf5a11208098f5d18905" } } $('.js-work-strip[data-work-id=30874026]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":30874026,"title":"Holocene glacial and colluvial activity in Leirungsdalen, eastern Jotunheimen, south-central Norway","translated_title":"","metadata":{"abstract":"Two terrestrial sections have been studied in order to reconstruct the Holocene glacial and colluvial history in Leirungsdalen, eastern Jotunheimen. The interpretation of individual sedimentary units is based on the grain-size distribution and compared with modern analogue samples collected in the respective streams and at sites close to the present glaciers. Stages of enhanced debris flow or glacial activity are recognized as sand and silt layers, respectively, while periods of low colluvial and glacial activity in the catchment are characterised by continuous peat accumulation. Age/depth curves based on radiocarbon dates from the Svarthammarbu and Steinflybekken sections indicate debris flow activity \u0026gt; 7500, 7300-6800,6600-5500, 5800, 5700, 5300-4900,4700, 4500,4300, 2300, 2100-1500, 1300, 700-600 and 500-400 cal. yr BP. The first Holocene glacial signal is detected ca. 5300 cal. yr BP. The frequency of glacial events seems to have increased during the Late Holocene, especially...","ai_title_tag":"Holocene Glacial History in Leirungsdalen","publication_name":"Norsk Geologisk Tidsskrift"},"translated_abstract":"Two terrestrial sections have been studied in order to reconstruct the Holocene glacial and colluvial history in Leirungsdalen, eastern Jotunheimen. The interpretation of individual sedimentary units is based on the grain-size distribution and compared with modern analogue samples collected in the respective streams and at sites close to the present glaciers. Stages of enhanced debris flow or glacial activity are recognized as sand and silt layers, respectively, while periods of low colluvial and glacial activity in the catchment are characterised by continuous peat accumulation. Age/depth curves based on radiocarbon dates from the Svarthammarbu and Steinflybekken sections indicate debris flow activity \u0026gt; 7500, 7300-6800,6600-5500, 5800, 5700, 5300-4900,4700, 4500,4300, 2300, 2100-1500, 1300, 700-600 and 500-400 cal. yr BP. The first Holocene glacial signal is detected ca. 5300 cal. yr BP. The frequency of glacial events seems to have increased during the Late Holocene, especially...","internal_url":"https://www.academia.edu/30874026/Holocene_glacial_and_colluvial_activity_in_Leirungsdalen_eastern_Jotunheimen_south_central_Norway","translated_internal_url":"","created_at":"2017-01-11T05:01:25.989-08:00","preview_url":null,"current_user_can_edit":null,"current_user_is_owner":null,"owner_id":33441460,"coauthors_can_edit":true,"document_type":"paper","co_author_tags":[],"downloadable_attachments":[{"id":51300462,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300462/thumbnails/1.jpg","file_name":"Holocene_glacial_and_colluvial_activity_20170111-6813-108sp5p.pdf","download_url":"https://www.academia.edu/attachments/51300462/download_file","bulk_download_file_name":"Holocene_glacial_and_colluvial_activity.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300462/Holocene_glacial_and_colluvial_activity_20170111-6813-108sp5p-libre.pdf?1484140117=\u0026response-content-disposition=attachment%3B+filename%3DHolocene_glacial_and_colluvial_activity.pdf\u0026Expires=1743853388\u0026Signature=ACiLdVjfr7Z-1rfBC73--WuzRNY9pxqZB8hP~26HdzOHaCmb50qQ0nvE2qnjKndSphELvR5PSs5CvIdETPznrIjA1QqomHHHb9Gu7KxeEBufG1paWAfarK9m0d0cbOwzddAt6~pvwHr5Wp3Cw-Q8AeaVt22CzV4096doLanlcZBUYUVVOulRf4kFlH~rEyfCra~ZykmhAtdWXBGM9XP1egxEQUrigHXyPEoi6CNnaO9J-6UwWZLMYiIDF5GLreA9yZW9OBWswBSrTDzg5-Retsh~HBCON0yOj9fqz3QbU4OA9ITt1SoDmwtgV1xHwfu2a6LAwogyVtduvtUif~GHuA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"slug":"Holocene_glacial_and_colluvial_activity_in_Leirungsdalen_eastern_Jotunheimen_south_central_Norway","translated_slug":"","page_count":17,"language":"en","content_type":"Work","summary":"Two terrestrial sections have been studied in order to reconstruct the Holocene glacial and colluvial history in Leirungsdalen, eastern Jotunheimen. The interpretation of individual sedimentary units is based on the grain-size distribution and compared with modern analogue samples collected in the respective streams and at sites close to the present glaciers. Stages of enhanced debris flow or glacial activity are recognized as sand and silt layers, respectively, while periods of low colluvial and glacial activity in the catchment are characterised by continuous peat accumulation. Age/depth curves based on radiocarbon dates from the Svarthammarbu and Steinflybekken sections indicate debris flow activity \u0026gt; 7500, 7300-6800,6600-5500, 5800, 5700, 5300-4900,4700, 4500,4300, 2300, 2100-1500, 1300, 700-600 and 500-400 cal. yr BP. The first Holocene glacial signal is detected ca. 5300 cal. yr BP. The frequency of glacial events seems to have increased during the Late Holocene, especially...","impression_tracking_id":null,"owner":{"id":33441460,"first_name":"Atle","middle_initials":null,"last_name":"Nesje","page_name":"AtleNesje","domain_name":"uib","created_at":"2015-07-29T13:25:19.080-07:00","display_name":"Atle Nesje","url":"https://uib.academia.edu/AtleNesje"},"attachments":[{"id":51300462,"title":"","file_type":"pdf","scribd_thumbnail_url":"https://attachments.academia-assets.com/51300462/thumbnails/1.jpg","file_name":"Holocene_glacial_and_colluvial_activity_20170111-6813-108sp5p.pdf","download_url":"https://www.academia.edu/attachments/51300462/download_file","bulk_download_file_name":"Holocene_glacial_and_colluvial_activity.pdf","bulk_download_url":"https://d1wqtxts1xzle7.cloudfront.net/51300462/Holocene_glacial_and_colluvial_activity_20170111-6813-108sp5p-libre.pdf?1484140117=\u0026response-content-disposition=attachment%3B+filename%3DHolocene_glacial_and_colluvial_activity.pdf\u0026Expires=1743853388\u0026Signature=ACiLdVjfr7Z-1rfBC73--WuzRNY9pxqZB8hP~26HdzOHaCmb50qQ0nvE2qnjKndSphELvR5PSs5CvIdETPznrIjA1QqomHHHb9Gu7KxeEBufG1paWAfarK9m0d0cbOwzddAt6~pvwHr5Wp3Cw-Q8AeaVt22CzV4096doLanlcZBUYUVVOulRf4kFlH~rEyfCra~ZykmhAtdWXBGM9XP1egxEQUrigHXyPEoi6CNnaO9J-6UwWZLMYiIDF5GLreA9yZW9OBWswBSrTDzg5-Retsh~HBCON0yOj9fqz3QbU4OA9ITt1SoDmwtgV1xHwfu2a6LAwogyVtduvtUif~GHuA__\u0026Key-Pair-Id=APKAJLOHF5GGSLRBV4ZA"}],"research_interests":[],"urls":[]}, dispatcherData: dispatcherData }); $(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874026-figures'); } }); </script> <div class="js-work-strip profile--work_container" data-work-id="30874025"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" rel="nofollow" href="https://www.academia.edu/30874025/Time_Series_at_Decadal_Resolution_Show_Tropical_Influence_on_Climate_Variability_in_The_Eastern_Nordic_Seas_Over_the_Past_2_Millenia"><img alt="Research paper thumbnail of Time Series at Decadal Resolution Show Tropical Influence on Climate Variability in The Eastern Nordic Seas Over the Past 2 Millenia" class="work-thumbnail" src="https://a.academia-assets.com/images/blank-paper.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title">Time Series at Decadal Resolution Show Tropical Influence on Climate Variability in The Eastern Nordic Seas Over the Past 2 Millenia</div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">Multi-proxy paleoclimatic time series have been developed from IMAGES Sites and adjacent suppleme...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">Multi-proxy paleoclimatic time series have been developed from IMAGES Sites and adjacent supplementary cores in the Eastern Norwegian Sea. The records cover the last 2000 years at decadal resolution, allowing for a detailed reconstruction of the surface hydrography of the main path of the northern limb of the north Atlantic circulation cell. Centennial to millennial scale events are recorded, such as the &quot;Medieval Warm Phase&quot; (MWP) and the &quot;Little Ice Age&quot; (LIA), which constitute the main long term century scale features. Superimposed on these are multidecadal variability of somewhat less amplitude. There is a close correspondance with continental records reflecting summer temperaure and winter precipitation in western Scandinavia over this period.SST changes are found to be in the range of 1-2 degrees. Significant land-sea correlation is observed. 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BP in the Smørstabbtinden massif of central Jotunheimen, southern Norway. Particular attention is paid to the century- to millennial-scale, pre-Little Ice Age glacial signal based on an estimated temporal resolution of ⩽55 and ⩽25 yr cm−1 for Bøvertunsvatnet and Dalsvatnet, respectively. Visible lithostratigraphic variations, organic content/loss-on-ignition, calcium carbonate content, magnetic susceptibility and grain-size fractions (especially the fine silt) are used as proxy indicators of glacier presence and extent in the lake catchments.Following deglaciation, the early Holocene was characterized by generally small glaciers until a major advance (the Finse Event) peaking at approximately 8200 cal. BP. From 7900 to at least 5300 cal. BP glaciers appear to have been absent from central Jotunheimen. 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BP in the Smørstabbtinden massif of central Jotunheimen, southern Norway. Particular attention is paid to the century- to millennial-scale, pre-Little Ice Age glacial signal based on an estimated temporal resolution of ⩽55 and ⩽25 yr cm−1 for Bøvertunsvatnet and Dalsvatnet, respectively. Visible lithostratigraphic variations, organic content/loss-on-ignition, calcium carbonate content, magnetic susceptibility and grain-size fractions (especially the fine silt) are used as proxy indicators of glacier presence and extent in the lake catchments.Following deglaciation, the early Holocene was characterized by generally small glaciers until a major advance (the Finse Event) peaking at approximately 8200 cal. BP. From 7900 to at least 5300 cal. BP glaciers appear to have been absent from central Jotunheimen. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-30874024-figures'); } }); </script> </div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="6140438" id="articles"><div class="js-work-strip profile--work_container" data-work-id="29829908"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/29829908/Flommer_og_flomskred_i_Gudbrandsdalen_i_et_v%C3%A6rmessig_og_klimatisk_perspektiv"><img alt="Research paper thumbnail of Flommer og flomskred i Gudbrandsdalen i et værmessig og klimatisk perspektiv" class="work-thumbnail" src="https://attachments.academia-assets.com/50300715/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/29829908/Flommer_og_flomskred_i_Gudbrandsdalen_i_et_v%C3%A6rmessig_og_klimatisk_perspektiv">Flommer og flomskred i Gudbrandsdalen i et værmessig og klimatisk perspektiv</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://uib.academia.edu/AtleNesje">Atle Nesje</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://uio.academia.edu/IngarM%C3%B8rkest%C3%B8lGundersen">Ingar Mørkestøl Gundersen</a>, and <a class="" data-click-track="profile-work-strip-authors" href="https://uio.academia.edu/RebeccaCannell">Rebecca J S Cannell</a></span></div><div class="wp-workCard_item"><span>Gård og utmark i Gudbrandsdalen - Arkeologiske undersøkelser i Fron 2011-2012</span><span>, 2016</span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">The archaeological investigations in the mid part of Gudbrandsdalen in 2011 and 2012 revealed a n...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">The archaeological investigations in the mid part of Gudbrandsdalen in 2011 and 2012 revealed a number of flood/avalanche horizons, of which «Forrskredet» (ca 350–200 BC), «Gammelofsen» (ca 50–1 BC), and «Merovingertidsofsen» (ca AD 600–800) were recognised as the major events at the investigated sites. Local topography and weather conditions (such as extreme weather events) and more long-term climatic trends were most likely the triggering factors for these events. During the time interval for Forrskredet, glaciers in Jotunheimen were in an advanced position, winter precipitation in mountains in western Norway (Jostedalsbreen) was relatively high, and summer temperatures in Scandinavia, as reconstructed from tree rings, were relatively high. Gammelofsen occurred during a period with relatively small glaciers in Jotunheimen as winter precipitation was increasing in western Norway and summer temperatures were rising in Scandinavia. During Merovingertidsofsen, glaciers in Jotunheimen were in an advanced position, winter precipitation was rapidly increasing in western Norway, and summer temperatures were relatively low in Scandinavia. The prehistoric flood and avalanche events in Gudbrandsdalen, such as the subsequent historic flood events, in particular «Storofsen» (1789) and «Storflaumen» (1860), certainly had a severe impact on settlement and farming.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="95422031346673aecc3f9d6469b20b68" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":50300715,"asset_id":29829908,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/50300715/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="29829908"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="29829908"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 29829908; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=29829908]").text(description); $(".js-view-count[data-work-id=29829908]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 29829908; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='29829908']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "95422031346673aecc3f9d6469b20b68" } } $('.js-work-strip[data-work-id=29829908]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":29829908,"title":"Flommer og flomskred i Gudbrandsdalen i et værmessig og klimatisk perspektiv","translated_title":"","metadata":{"abstract":"The archaeological investigations in the mid part of Gudbrandsdalen in 2011 and 2012 revealed a number of flood/avalanche horizons, of which «Forrskredet» (ca 350–200 BC), «Gammelofsen» (ca 50–1 BC), and «Merovingertidsofsen» (ca AD 600–800) were recognised as the major events at the investigated sites. Local topography and weather conditions (such as extreme weather events) and more long-term climatic trends were most likely the triggering factors for these events. During the time interval for Forrskredet, glaciers in Jotunheimen were in an advanced position, winter precipitation in mountains in western Norway (Jostedalsbreen) was relatively high, and summer temperatures in Scandinavia, as reconstructed from tree rings, were relatively high. Gammelofsen occurred during a period with relatively small glaciers in Jotunheimen as winter precipitation was increasing in western Norway and summer temperatures were rising in Scandinavia. During Merovingertidsofsen, glaciers in Jotunheimen were in an advanced position, winter precipitation was rapidly increasing in western Norway, and summer temperatures were relatively low in Scandinavia. 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$(this).data('initialized', true); } }); $a.trackClickSource(".js-work-strip-work-link", "profile_work_strip") if (false) { Aedu.setUpFigureCarousel('profile-work-29829908-figures'); } }); </script> </div><div class="profile--tab_content_container js-tab-pane tab-pane" data-section-id="6140585" id="books"><div class="js-work-strip profile--work_container" data-work-id="29830203"><div class="profile--work_thumbnail hidden-xs"><a class="js-work-strip-work-link" data-click-track="profile-work-strip-thumbnail" href="https://www.academia.edu/29830203/G%C3%A5rd_og_utmark_i_Gudbrandsdalen_Arkeologiske_unders%C3%B8kelser_i_Fron_2011_2012"><img alt="Research paper thumbnail of Gård og utmark i Gudbrandsdalen - Arkeologiske undersøkelser i Fron 2011-2012" class="work-thumbnail" src="https://attachments.academia-assets.com/50301241/thumbnails/1.jpg" /></a></div><div class="wp-workCard wp-workCard_itemContainer"><div class="wp-workCard_item wp-workCard--title"><a class="js-work-strip-work-link text-gray-darker" data-click-track="profile-work-strip-title" href="https://www.academia.edu/29830203/G%C3%A5rd_og_utmark_i_Gudbrandsdalen_Arkeologiske_unders%C3%B8kelser_i_Fron_2011_2012">Gård og utmark i Gudbrandsdalen - Arkeologiske undersøkelser i Fron 2011-2012</a></div><div class="wp-workCard_item wp-workCard--coauthors"><span>by </span><span><a class="" data-click-track="profile-work-strip-authors" href="https://uio.academia.edu/IngarM%C3%B8rkest%C3%B8lGundersen">Ingar Mørkestøl Gundersen</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/JanHenningLarsen">Jan Henning Larsen</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/OleChristianL%C3%B8naas">Ole Christian Lønaas</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://uib.academia.edu/AtleNesje">Atle Nesje</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://uio.academia.edu/RebeccaCannell">Rebecca J S Cannell</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://ntnu-no.academia.edu/KristinEriksen">Kristin Eriksen</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://niku.academia.edu/LiseLoktu">Lise Loktu</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/TVillumsen">Tina Villumsen</a>, <a class="" data-click-track="profile-work-strip-authors" rel="nofollow" href="https://independent.academia.edu/ArneJouttij%C3%A4rvi">Arne Jouttijärvi</a>, <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/AnnineMoltsen">Annine Moltsen</a>, and <a class="" data-click-track="profile-work-strip-authors" href="https://independent.academia.edu/RichardMacphail">Richard Macphail</a></span></div><div class="wp-workCard_item"><span class="js-work-more-abstract-truncated">E6-prosjektet Gudbrandsdalen er det mest omfattende utgravningsprosjektet som er gjennomført i Op...</span><a class="js-work-more-abstract" data-broccoli-component="work_strip.more_abstract" data-click-track="profile-work-strip-more-abstract" href="javascript:;"><span> more </span><span><i class="fa fa-caret-down"></i></span></a><span class="js-work-more-abstract-untruncated hidden">E6-prosjektet Gudbrandsdalen er det mest omfattende utgravningsprosjektet som er gjennomført i Oppland noensinne, og har sin bakgrunn i etableringen av ny E6 gjennom dalføret. I 2011 og 2012 gjennomførte Kulturhistorisk museum utgravninger på 64 steder i kommunene Sør-Fron, Nord-Fron og Sel, og utgravningene avdekket blant annet en frem til da ukjent flom-, bosetnings-og jordbrukshistorikk. Omfattende undersøkelser ble også gjort i utmarka, der et stort antall kull-og fangstgroper ble gravd ut. Det samlede vitenska-pelige materialet fra prosjektet har endret forståelsen av Gudbrandsdalens arkeologi og gitt ny kunnskap om hvordan samfunnet i dalføret utviklet seg i jernalderen og middelalderen. Denne boken presenterer de viktigste faglige resultatene, setter resultatene inn i en større kulturhistorisk sammenheng og gjør rede for kunnskapsstatusen på viktige fagområder innenfor Gudbrandsdalens arkeologi.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="26d9e96d421df7975efbed293fd8c8e4" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":50301241,"asset_id":29830203,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/50301241/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="29830203"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="29830203"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 29830203; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=29830203]").text(description); $(".js-view-count[data-work-id=29830203]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 29830203; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='29830203']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "26d9e96d421df7975efbed293fd8c8e4" } } $('.js-work-strip[data-work-id=29830203]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":29830203,"title":"Gård og utmark i Gudbrandsdalen - Arkeologiske undersøkelser i Fron 2011-2012","translated_title":"","metadata":{"abstract":"E6-prosjektet Gudbrandsdalen er det mest omfattende utgravningsprosjektet som er gjennomført i Oppland noensinne, og har sin bakgrunn i etableringen av ny E6 gjennom dalføret. 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When rescued by systematic fieldwork (glacial archaeology), this evidence opens an unprecedented window on the chronology of high-elevation activity. Recent research in Jotunheimen and surrounding mountain areas of Norway has recovered over 2000 finds—many associated with reindeer hunting (e.g. arrows). We report the radiocarbon dates of 153 objects and use a kernel density estimation (KDE) method to determine the distribution of dated events from ca 4000 BCE to the present. Interpreted in light of shifting environmental, preservation and socioeconomic factors, these new data show counterintuitive trends in the intensity of reindeer hunting and other high-elevation activity. Cold temperatures may sometimes have kept humans from Norway's highest elevations, as expected based on accessibility, exposure and reindeer distributions. In times of increasing demand for mountain resources, however, activity probably continued in the face of adverse or variable climatic conditions. The use of KDE modelling makes it possible to observe this patterning without the spurious effects of noise introduced by the discrete nature of the finds and<br />the radiocarbon calibration process.</span></div><div class="wp-workCard_item wp-workCard--actions"><span class="work-strip-bookmark-button-container"></span><a id="6aedb074a5bed01f2abc81c3136ed180" class="wp-workCard--action" rel="nofollow" data-click-track="profile-work-strip-download" data-download="{"attachment_id":55621414,"asset_id":35746378,"asset_type":"Work","button_location":"profile"}" href="https://www.academia.edu/attachments/55621414/download_file?s=profile"><span><i class="fa fa-arrow-down"></i></span><span>Download</span></a><span class="wp-workCard--action visible-if-viewed-by-owner inline-block" style="display: none;"><span class="js-profile-work-strip-edit-button-wrapper profile-work-strip-edit-button-wrapper" data-work-id="35746378"><a class="js-profile-work-strip-edit-button" tabindex="0"><span><i class="fa fa-pencil"></i></span><span>Edit</span></a></span></span></div><div class="wp-workCard_item wp-workCard--stats"><span><span><span class="js-view-count view-count u-mr2x" data-work-id="35746378"><i class="fa fa-spinner fa-spin"></i></span><script>$(function () { var workId = 35746378; window.Academia.workViewCountsFetcher.queue(workId, function (count) { var description = window.$h.commaizeInt(count) + " " + window.$h.pluralize(count, 'View'); $(".js-view-count[data-work-id=35746378]").text(description); $(".js-view-count[data-work-id=35746378]").attr('title', description).tooltip(); }); });</script></span></span><span><span class="percentile-widget hidden"><span class="u-mr2x work-percentile"></span></span><script>$(function () { var workId = 35746378; window.Academia.workPercentilesFetcher.queue(workId, function (percentileText) { var container = $(".js-work-strip[data-work-id='35746378']"); container.find('.work-percentile').text(percentileText.charAt(0).toUpperCase() + percentileText.slice(1)); container.find('.percentile-widget').show(); container.find('.percentile-widget').removeClass('hidden'); }); });</script></span></div><div id="work-strip-premium-row-container"></div></div></div><script> require.config({ waitSeconds: 90 })(["https://a.academia-assets.com/assets/wow_profile-a9bf3a2bc8c89fa2a77156577594264ee8a0f214d74241bc0fcd3f69f8d107ac.js","https://a.academia-assets.com/assets/work_edit-ad038b8c047c1a8d4fa01b402d530ff93c45fee2137a149a4a5398bc8ad67560.js"], function() { // from javascript_helper.rb var dispatcherData = {} if (true){ window.WowProfile.dispatcher = window.WowProfile.dispatcher || _.clone(Backbone.Events); dispatcherData = { dispatcher: window.WowProfile.dispatcher, downloadLinkId: "6aedb074a5bed01f2abc81c3136ed180" } } $('.js-work-strip[data-work-id=35746378]').each(function() { if (!$(this).data('initialized')) { new WowProfile.WorkStripView({ el: this, workJSON: {"id":35746378,"title":"The chronology of reindeer hunting on Norway's highest ice patches","translated_title":"","metadata":{"abstract":"The melting of perennial ice patches globally is uncovering a fragile record of alpine activity, especially hunting and the use of mountain passes. 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