On the Automated Mapping of Snow Cover on Glaciers and Calculation of Snow Line Altitudes from Multi-Temporal Landsat Data
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Snow Depth on Arctic Sea Ice
1814 JOURNAL OF CLIMATE VOLUME 12 Snow Depth on Arctic Sea Ice STEPHEN G. WARREN,IGNATIUS G. RIGOR, AND NORBERT UNTERSTEINER Department of Atmospheric Sciences, University of Washington, Seattle, Washington VLADIMIR F. R ADIONOV,NIKOLAY N. BRYAZGIN, AND YEVGENIY I. ALEKSANDROV Arctic and Antarctic Research Institute, St. Petersburg, Russia ROGER COLONY International Arctic Research Center, University of Alaska, Fairbanks, Alaska (Manuscript received 5 December 1997, in ®nal form 27 July 1998) ABSTRACT Snow depth and density were measured at Soviet drifting stations on multiyear Arctic sea ice. Measurements were made daily at ®xed stakes at the weather station and once- or thrice-monthly at 10-m intervals on a line beginning about 500 m from the station buildings and extending outward an additional 500 or 1000 m. There were 31 stations, with lifetimes of 1±7 yr. Analyses are performed here for the 37 years 1954±91, during which time at least one station was always reporting. Snow depth at the stakes was sometimes higher than on the lines, and sometimes lower, but no systematic trend of snow depth was detected as a function of distance from the station along the 1000-m lines that would indicate an in¯uence of the station. To determine the seasonal progression of snow depth for each year at each station, priority was given to snow lines if available; otherwise the ®xed stakes were used, with an offset applied if necessary. The ice is mostly free of snow during August. Snow accumulates rapidly in September and October, moderately in November, very slowly in December and January, then moderately again from February to May. -
Comparison of Remote Sensing Extraction Methods for Glacier Firn Line- Considering Urumqi Glacier No.1 As the Experimental Area
E3S Web of Conferences 218, 04024 (2020) https://doi.org/10.1051/e3sconf/202021804024 ISEESE 2020 Comparison of remote sensing extraction methods for glacier firn line- considering Urumqi Glacier No.1 as the experimental area YANJUN ZHAO1, JUN ZHAO1, XIAOYING YUE2and YANQIANG WANG1 1College of Geography and Environmental Science, Northwest Normal University, Lanzhou, China 2State Key Laboratory of Cryospheric Sciences, Northwest Institute of Eco-Environment and Resources/Tien Shan Glaciological Station, Chinese Academy of Sciences, Lanzhou, China Abstract. In mid-latitude glaciers, the altitude of the snowline at the end of the ablating season can be used to indicate the equilibrium line, which can be used as an approximation for it. In this paper, Urumqi Glacier No.1 was selected as the experimental area while Landsat TM/ETM+/OLI images were used to analyze and compare the accuracy as well as applicability of the visual interpretation, Normalized Difference Snow Index, single-band threshold and albedo remote sensing inversion methods for the extraction of the firn lines. The results show that the visual interpretation and the albedo remote sensing inversion methods have strong adaptability, alonger with the high accuracy of the extracted firn line while it is followed by the Normalized Difference Snow Index and the single-band threshold methods. In the year with extremely negative mass balance, the altitude deviation of the firn line extracted by different methods is increased. Except for the years with extremely negative mass balance, the altitude of the firn line at the end of the ablating season has a good indication for the altitude of the balance line. -
Glacier (And Ice Sheet) Mass Balance
Glacier (and ice sheet) Mass Balance The long-term average position of the highest (late summer) firn line ! is termed the Equilibrium Line Altitude (ELA) Firn is old snow How an ice sheet works (roughly): Accumulation zone ablation zone ice land ocean • Net accumulation creates surface slope Why is the NH insolation important for global ice• sheetSurface advance slope causes (Milankovitch ice to flow towards theory)? edges • Accumulation (and mass flow) is balanced by ablation and/or calving Why focus on summertime? Ice sheets are very sensitive to Normal summertime temperatures! • Ice sheet has parabolic shape. • line represents melt zone • small warming increases melt zone (horizontal area) a lot because of shape! Slightly warmer Influence of shape Warmer climate freezing line Normal freezing line ground Furthermore temperature has a powerful influence on melting rate Temperature and Ice Mass Balance Summer Temperature main factor determining ice growth e.g., a warming will Expand ablation area, lengthen melt season, increase the melt rate, and increase proportion of precip falling as rain It may also bring more precip to the region Since ablation rate increases rapidly with increasing temperature – Summer melting controls ice sheet fate* – Orbital timescales - Summer insolation must control ice sheet growth *Not true for Antarctica in near term though, where it ʼs too cold to melt much at surface Temperature and Ice Mass Balance Rule of thumb is that 1C warming causes an additional 1m of melt (see slope of ablation curve at right) -
Étude Sur Le Glacier Noir Et Le Glacier Blanc Dans Le Massif Du
Étude sur le glacier Noir et le glacier Blanc dans le massif du Pelvoux : [rapport sur les observations rassemblées en août 1904 dans les Alpes du Dauphiné] Charles Jacob, G. Flusin To cite this version: Charles Jacob, G. Flusin. Étude sur le glacier Noir et le glacier Blanc dans le massif du Pelvoux : [rapport sur les observations rassemblées en août 1904 dans les Alpes du Dauphiné]. 1905. insu- 01068516 HAL Id: insu-01068516 https://hal-insu.archives-ouvertes.fr/insu-01068516 Submitted on 25 Sep 2014 HAL is a multi-disciplinary open access L’archive ouverte pluridisciplinaire HAL, est archive for the deposit and dissemination of sci- destinée au dépôt et à la diffusion de documents entific research documents, whether they are pub- scientifiques de niveau recherche, publiés ou non, lished or not. The documents may come from émanant des établissements d’enseignement et de teaching and research institutions in France or recherche français ou étrangers, des laboratoires abroad, or from public or private research centers. publics ou privés. ' ÉTUDE SUR LK GLACIER NOIR ET LE GLACIER BLANC DANS LE MASSIF DU PELVOUX HOMMAGE DE lA COMMISSION COMMISSION FRANÇAISE DES GLACIERS ÉTUDE sun LE GL�CIER NOIR ET LE GLACIER BLANC DANS LE MASSIF DU PELVOUX PAR MM. CHARLES JACOB ET GEORGES FLUSIN Avec 2 planches phototypiques Et :! cartes topographiques au 1/10.000• DIIESSÉES PAH i\Œ. LAFA Y, FLUSIN et JACOB RAPPORT SUR LES OBSERVA'I'IONS RASSEMBLÉES EN AOÛT 1004 DANS LES ALPES DU DAUPHINÉ Avec te concours de la Société des Touristes du Dauphiné lh� Ministère de l'Agriculture Et du llfinistère de t'In.çtruction publique Extrait de l'Annuaire de la Société des Touristes du Dauphiné Numéro 30, 190� ----- �----- GRENOBLE TTJ>OGHAPHIE ET I.ITHOGHAI'HIE AI.Lllo:H FRÈRES 26, Cours de Saint-André, 26 1905 ÉTUDE SUR LE GLACIER NOIR ET LE GLACIER BLi\NC DANS LE MASSIF DU PELVOUX INTRODUCTION Le soin de poursuivre, pour· le compte de la Commis sion française, l'étude des glaciers du Dauphiné a été laissé cette armée à MM. -
Snow Cover and Glacier Change Study in Nepalese Himalaya Using Remote Sensing and Geographic Information System
26 A. B. Shrestha & S. P. Joshi August 2009 Snow Cover and Glacier Change Study in Nepalese Himalaya Using Remote Sensing and Geographic Information System Arun Bhakta Shrestha1 and Sharad Prasad Joshi2 1 International Centre for Integrated Mountain Development, Nepal E-mail: [email protected] 2 Water and Energy Commission Secretariat, Nepal ABSTRACT Snow cover and glaciers in the Himalaya play a major role in the generation of stream flow in south Asia. Various studies have suggested that the glaciers in the Himalaya are in general condition of retreat. The snowline is also found to be retreating. While there are relatively more studies on glaciers fluctuation in the Himalaya, studies on snow cover is relatively sparse. In this study, snow cover and glacier fluctuation in the Nepalese Himalaya were studied using remote sensing techniques and geographic information system. The study was carried out in two spatial scales: catchments scale and national scale. In catchments scale two catchments: Langtang and Khumbu were studied. Intermittent medium resolution satellite imageries (Landsat) were used to study the fluctuation in snow cover and glacier area in the two catchments. In the national scale study coarse resolution (MODIS) imageries were used to derive seasonal variations in snow cover. An indication of decreasing trend in snow cover is shown by this study, although this result needs verification with more data. The snowline elevation is in general higher in Khumbu compared to Langtang. In both catchments, snowline elevation are higher in east, south-east, south and south-west aspects. The areas of snow cover in those aspects are also greater. -
World Map Outline Find and Shade: Andes, Alps, Rockies, Himalayas, Caucasus Mountains, East Africa Mountains, Alaska/Yukon Ranges, Sentinel Range, Sudiman Range
World Map Outline Find and shade: Andes, Alps, Rockies, Himalayas, Caucasus Mountains, East Africa Mountains, Alaska/Yukon Ranges, Sentinel Range, Sudiman Range 1 The World’s Highest Peaks 2 Earth Cross-Section 3 Mountain Climates Fact Sheet • How high a mountain is affects what its climate is like. Moving 300 metres up is the same as moving 350 miles towards one of the poles! • Air pressure also changes as one gains altitude. At the top of Mount Everest (8848 m) the pressure is around 310-360 millibars, compared to around 1013 mb at sea level. • As a result of falling air pressure, rising air expands and cools (although, dry air cools faster than moist air because, as the moist air rises, the water vapour condenses – like in clouds – and this gives off some heat). The higher you are the cooler it gets. That is why we often have snow on mountaintops, even along the equator. • Mountains therefore act as a barrier to moisture-laden winds. Air rising to pass over the mountains cools and the water vapour condenses, turning into either clouds, rain, or if it is cold enough, snow. This is why on one side of a mountain you can experience a wet climate, while on the other side of the same mountain you find an arid one. • A large mountain range can affect the weather of the land beyond it. The Himalayas influence the climate of the rest of India by sheltering it from the cold air mass of central Asia. • In high mountains the first snow may fall several weeks earlier than it does in the surrounding area. -
Status of the Cordillera Vilcanota, Including the Quelccaya Ice Cap, Northern Central Andes, Peru
The Cryosphere, 8, 359–376, 2014 Open Access www.the-cryosphere.net/8/359/2014/ doi:10.5194/tc-8-359-2014 The Cryosphere © Author(s) 2014. CC Attribution 3.0 License. Glacial areas, lake areas, and snow lines from 1975 to 2012: status of the Cordillera Vilcanota, including the Quelccaya Ice Cap, northern central Andes, Peru M. N. Hanshaw and B. Bookhagen Department of Geography, University of California, Santa Barbara, CA, USA Correspondence to: M. N. Hanshaw ([email protected]) Received: 14 December 2012 – Published in The Cryosphere Discuss.: 25 February 2013 Revised: 19 December 2013 – Accepted: 10 January 2014 – Published: 3 March 2014 Abstract. Glaciers in the tropical Andes of southern Peru as glacial regions have decreased, 77 % of lakes connected have received limited attention compared to glaciers in to glacial watersheds have either remained stable or shown other regions (both near and far), yet remain of vital im- a roughly synchronous increase in lake area, while 42 % of portance to agriculture, fresh water, and hydropower sup- lakes not connected to glacial watersheds have declined in plies of downstream communities. Little is known about area (58 % have remained stable). Our new and detailed data recent glacial-area changes and how the glaciers in this on glacial and lake areas over 37 years provide an important region respond to climate changes, and, ultimately, how spatiotemporal assessment of climate variability in this area. these changes will affect lake and water supplies. To rem- These data can be integrated into further studies to analyze edy this, we have used 158 multi-spectral satellite images inter-annual glacial and lake-area changes and assess hydro- spanning almost 4 decades, from 1975 to 2012, to ob- logic dependence and consequences for downstream popula- tain glacial- and lake-area outlines for the understudied tions. -
Learning About Precipitation Orographic Enhancement from Snow-Course Data Improves Water-Balance Modeling
https://doi.org/10.5194/hess-2020-571 Preprint. Discussion started: 26 November 2020 c Author(s) 2020. CC BY 4.0 License. Learning about precipitation orographic enhancement from snow-course data improves water-balance modeling Francesco Avanzi1, Giulia Ercolani1, Simone Gabellani1, Edoardo Cremonese2, Paolo Pogliotti2, Gianluca Filippa2, Umberto Morra di Cella2,1, Sara Ratto3, Hervè Stevenin3, Marco Cauduro4, and Stefano Juglair4 1CIMA Research Foundation, Via Armando Magliotto 2, 17100 Savona, Italy 2Climate Change Unit, Environmental Protection Agency of Aosta Valley, Loc. La Maladière, 48-11020 Saint-Christophe, Italy 3Regione Autonoma Valle d’Aosta, Centro funzionale regionale, Via Promis 2/a, 11100 Aosta, Italy 4Direzione Operativa Operations, C.V.A. S.p.A., Via Stazione 31, 11024 Châtillon, Italy Correspondence: Francesco Avanzi ([email protected]) Abstract. Precipitation orographic enhancement depends on both synoptic circulation and topography. Since high-elevation headwaters are often sparsely instrumented, the magnitude and distribution of this enhancement remain poorly understood. Filling this knowledge gap would allow a significant step ahead for hydrologic-forecasting procedures and water management in general. 5 Here, we hypothesized that spatially distributed, manual measurements of snow depth (courses) could provide new insights into this process. We leveraged 11,000+ snow-course data upstream two reservoirs in the Western European Alps (Aosta Valley, Italy) to estimate precipitation orographic enhancement in the form of lapse rates and consequently improve predictions of a snow-hydrologic modeling chain (Flood-PROOFS). We found that Snow Water Equivalent (SWE) above 3000 m ASL was between 2 and 8.5 times higher than recorded cumulative seasonal precipitation below 1000 m ASL, with gradients up to 1000 1 10 mm w.e. -
Aberystwyth University Glaciological and Geomorphological Map
Aberystwyth University Glaciological and geomorphological map of Glacier Noir and Glacier Blanc, French Alps Lardeux, Pierre; Glasser, Neil; Holt, Tom; Hubbard, Bryn Published in: Journal of Maps DOI: 10.1080/17445647.2015.1054905 Publication date: 2016 Citation for published version (APA): Lardeux, P., Glasser, N., Holt, T., & Hubbard, B. (2016). Glaciological and geomorphological map of Glacier Noir and Glacier Blanc, French Alps. Journal of Maps, 12(3), 582-596. https://doi.org/10.1080/17445647.2015.1054905 General rights Copyright and moral rights for the publications made accessible in the Aberystwyth Research Portal (the Institutional Repository) are retained by the authors and/or other copyright owners and it is a condition of accessing publications that users recognise and abide by the legal requirements associated with these rights. • Users may download and print one copy of any publication from the Aberystwyth Research Portal for the purpose of private study or research. • You may not further distribute the material or use it for any profit-making activity or commercial gain • You may freely distribute the URL identifying the publication in the Aberystwyth Research Portal Take down policy If you believe that this document breaches copyright please contact us providing details, and we will remove access to the work immediately and investigate your claim. tel: +44 1970 62 2400 email: [email protected] Download date: 03. Oct. 2019 1 1 Glaciological and geomorphological map of 2 Glacier Noir and Glacier Blanc, French Alps 3 This is an Accepted Manuscript of an article published by Taylor & Francis Group in 4 Journal of Maps on 17th June 2015, available online: 5 http://www.tandfonline.com/doi/full/10.1080/17445647.2015.1054905 6 Abstract 7 This paper presents and describes a glaciological and geomorphological map of Glacier Noir and 8 Glacier Blanc, French Alps. -
Maps of Snow-Cover Probability for the Northern Hemisphere
June 1967 R. R. Dickson and Julian Posey 347 MAPS OF SNOW-COVER PROBABILITY FOR THE NORTHERN HEMISPHERE R.R. DICKSON AND JULIAN POSEY Extended Forecast Division; NMC, Weather Bureau, ESSA, Washington, D.C. ABSTRACT Map analyses are provided depicting the probability of snow-cover 1 inch or more in depth at the end of each month from September through May for the Northern Hemisphere. 1. INTRODUCTION To supplement this primary data source, empirical snow-cover probabilities were computed for the 193 1-50 Recent work dealing with thermodynamic [l] and period for a network of 110 stations in the United States synoptic [8] aspects of long-range forecasting has em- from data included in US. Weather Bureau Station phasized the importance of considering the heat balance Record Books (available on microfilm from the Atmos- of the earth and the atmosphere when dealing with the pheric Sciences Library of ESSA) . Canadian snow-cover long-term evolution of the atmospheric circulation. data were extracted from a recent publication [lo]. This An important factor in such a heat balance is the albedo was augmented for May and September by data from of the earth’s surface and this in turn is critically depend- additional stations during 1940-64, obtained from monthly ent upon the snow-cover distribution. published records [5]. Thus a need exists for broadscale climatic analyses Analyses for China and Korea are based upon data depicting the areal extent of snow cover throughout the published by their respective meteorological offices [9] , [4]. year. While map analyses of average snow depth and Both sources give the a$erage number of days with snow average dates of first and last snowfall are readily available, cover for each month. -
PDF Preview of Snow and Mixed Climbs Ecrins East
5 Valloire Albertville ECRINS EAST, CERCES, QUEYRAS, D902 ACCESS ROADS MAP N Grenoble Lyon Col du Galibier La Grave Col du Lautaret 5-CLAREE5-CLAREE Italy Villar Névache Fréjus & d'Arêne Mont-Blanc tunnels D994 4-GUISANE4-GUISANE Monêtier-les-Bains S24 D109 Col du 1 Montgenevre N94 Ailefroide Briançon Puy Chalvin Cervières 3-VALLOUISE3-VALLOUISE Villar Saint-Pancrace Vallouise D902 D4 D994E 6-BRIANCON6-BRIANCON Col de l'Isoard N94 2-FOURNEL2-FOURNEL D638 D947 L'Argentière-La-Bessée D5 Col Molines Agnel D902 Mont- VOLUME II Dauphin D60 Ceillac ECRINS WEST Guillestre 7-GUIL7-GUIL D638 Saint-Clément N94 St Marcellin 1-EMBRUN1-EMBRUN D39 D902 Embrun Crevoux N94 Col de Vars Gap Marseille VALLOUISE - Bans Valley - 31 LES BANS Glacier 0 km 0,5 km 1km des 21 Bans Névé Contreforts Scale Ovale des Bans N Brèche des Bans - 18 20 Pic des BV ANS alley Aupillous 17 Pas 15-16 Glacieracier du SellarSeSella Entraygues des Aupillous Bans hut 1624 m 14 2083 m Torrent des Bans Col du Sellar 12-13 GlacierGlacier de Pic Jocelme Bonvoisinn 8-9 10-11 Brèche de Bonvoisin Glacier des Bruyères Glacier de VALLOUISE Pic de Bonvoisin 5 - 7 l'Amirée VOLUME II Malamort WEST Crête de Aulp ValleyMartin Brèche des Bruyères Pic de Malamort Vallon des Bans Access to this valley is very long in winter conditions. The best way of reducing the walk in is to wait for good conditions in late autumn/early winter or in spring, when the road is open at least as far as the Chapelle de Béassac (1472 m), and sometimes as far as Entraygues (1625 m). -
Glacier Noir Jusqu'aux Balmes De François Blanc
Glacier Noir jusqu'aux Balmes de François Blanc Une randonnée proposée par Britanicus100 Parcours de haute montagne conduisant sur le fil d'une crête morainique avec panorama époustouflant sur les hautes cimes des Écrins. Randonnée n°276518 Durée : 4h10 Difficulté : Moyenne Distance : 7.92km Retour point de départ : Oui Dénivelé positif : 673m Activité : A pied Dénivelé négatif : 673m Régions : Alpes, Ecrins, Dauphiné Point haut : 2551m Commune : Pelvoux (05340) Point bas : 1878m Description De Vallouise, emprunter la D994E en direction d’Ailefroide puis du Pré de Points de passages Madame Carle. Stationner sur le parking situé près du chalet refuge. Droit d’entrée au parking de 2€. D/A Parking de Madame Carle N 44.918062° / E 6.415775° - alt. 1878m - km 0 (D/A) Du Refuge de Madame Carle, emprunter l’allée au Nord-Ouest en direction des glaciers. 1 Carrefour de sentiers, panneau Glacier Noir N 44.923702° / E 6.406574° - alt. 2053m - km 1.36 Celle-ci traverse le torrent de la Momie et celui du Glacier Noir puis monte en lacets. 2 Balmes de François Blanc N 44.918548° / E 6.383874° - alt. 2449m - km 3.34 (1) Au troisième lacet et au panneau (cote de 2040m), laisser à droite le sentier du Glacier Blanc pour prendre à gauche celui du Glacier Noir. 3 Point le plus élevé N 44.917951° / E 6.376287° - alt. 2551m - km 3.96 Le sentier monte régulièrement de façon rectiligne sur le fil de la crête de la moraine avec à gauche le Glacier Noir et à droite le Ravin de l’Encoula.