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  • 1
    Online Resource
    Online Resource
    Cambridge :Cambridge University Press,
    Keywords: Climatic changes. ; Electronic books.
    Description / Table of Contents: Applying an interdisciplinary methodology, this comprehensive book provides a definitive overview of the major high-mountain systems worldwide, giving unprecedented insights into global drivers of high-mountain cryosphere change and their implications for people across high-mountain regions. An invaluable reference for researchers and professionals in cryospheric science, geomorphology, climatology and environmental studies.
    Type of Medium: Online Resource
    Pages: 1 online resource (378 pages)
    Edition: 1st ed.
    ISBN: 9781316363553
    DDC: 577.5/3
    Language: English
    Note: Cover -- Half-title -- Title page -- Copyright information -- Table of contents -- List of contributors -- Acknowledgments -- 1 Introduction: human-environment dynamics in the high-mountain cryosphere -- References -- Part I Global drivers -- 2 Influence of climate variability and large-scale circulation on the mountain cryosphere -- 2.1 Introduction -- 2.2 European mountains -- 2.3 North American Cordillera -- 2.4 Tibetan Plateau and the surrounding high-mountain ranges -- 2.5 The tropical Andes -- 2.6 Mt. Kilimanjaro: a case study from East Africa -- 2.7 Conclusions -- Acknowledgements -- References -- 3 Temperature, precipitation and related extremes in mountain areas -- 3.1 Introduction -- 3.2 Basic characteristics of near surface temperature in mountain topography -- 3.2.1 Altitude dependence of 2m temperature -- 3.2.2 Altitude dependence of daily temperature anomalies -- 3.2.3 The relation between surface air pressure and 2m temperature -- 3.3 Temperature extremes -- 3.4 Precipitation patterns in mountain areas -- 3.4.1 Measuring and monitoring precipitation -- 3.5 Precipitation extremes -- 3.5.1 Selected gridded data products -- 3.5.1.1 Reanalyses -- 3.5.1.2 Combined observations -- 3.5.1.3 Interpolated rain-gauge station data -- 3.5.2 Comparison and discussion of the gridded data products -- 3.6 Conclusions -- Acknowledgments -- References -- 4 Snow and avalanches -- 4.1 Introduction -- 4.1.1 Snow cover -- 4.1.2 Snow avalanche hazard and risk -- 4.2 Environmental change -- 4.2.1 Climate change and mountain snow cover -- 4.2.2 Effects on snow avalanches -- 4.3 Socio-economic change -- 4.3.1 Drivers of socio-economic change -- 4.3.2 Effects on snow avalanche risk -- 4.3.2.1 Temporal dynamics of socio-economic changes -- 4.3.2.2 Spatial dynamics of socio-economic changes -- 4.4 Conclusions -- References. , 5 The frozen frontier: the extractives super cycle in a time of glacier recession -- 5.1 Introduction -- 5.2 The icy edge of climate change -- 5.3 The icy edge of the global extractives super cycle -- 5.4 New mountains of mines and the frozen north -- 5.5 Extending the extractives complex into the cryosphere -- 5.6 Liquid relations and stratified societies -- 5.7 The frigid fringe: extractive bio-futures and the freezing depths -- 5.8 Conclusion -- References -- 6 Cultural values of glaciers -- 6.1 Introduction -- 6.2 Three cases in the Alps, the Andes, and the North Cascades -- 6.3 Understanding the cultural values of glaciers -- 6.4 Case study 1: Stilfs, South Tirol, Italian Alps -- 6.4.1 The role of glaciers for community, identity, and self-reliance in Stilfs -- 6.5 Case study 2: Siete Imperios, Cordillera Blanca, Peru -- 6.5.1 The role of glaciers and mountains for community, identity, and self-reliance in Siete Imperios -- 6.6 Case study 3: Glacier and Concrete, North Cascades, USA -- 6.6.1 The role of glaciers and mountains for community, identity, and self-reliance in Glacier and Concrete -- 6.7 Discussion and conclusions -- Acknowledgments -- References -- Part II Processes -- 7 Implications for hazard and risk of seismic and volcanic responses to climate change in the high-mountain cryosphere -- 7.1 Introduction -- 7.2 Ice retreat and earthquakes -- 7.3 The hazard consequences of ice retreat in volcanic landscapes -- 7.4 Future risk to society and economy and potential impacts -- 7.4.1 The seismic threat -- 7.4.2 The volcanic threat -- 7.5 Conclusions -- References -- 8 Catastrophic mass wasting in high mountains -- 8.1 Introduction -- 8.2 More mass wasting because of climate change? -- 8.3 The search for causes and triggers -- 8.4 The rockslide-glacier couple -- 8.5 Rare and rapid mixtures -- 8.6 The forgotten mountains. , 8.7 Conclusions and scope for future research -- Acknowledgements -- References -- 9 Glacier- and permafrost-related slope instabilities -- 9.1 Introduction -- 9.1.1 Cryospheric rock slope systems -- 9.1.2 Prerequisites for instability -- 9.2 Glacially induced preconditioning and conditioning of alpine rock slopes -- 9.2.1 Preconditioning by long-term erosional processes -- 9.2.2 Temporal and spatial patterns of post-glacial rock slope instability -- 9.3 Permafrost-induced preconditioning and conditioning of alpine rock slopes -- 9.3.1 Instability assessment of permafrost-affected slopes -- 9.3.2 Temporal and spatial controls of permafrost-affected rock slope failure -- 9.3.2.1 Increased shear stress -- 9.3.2.2 Reduced shear resistance -- 9.4 Present-day and anticipated response of para- and periglacial rock slope systems -- 9.4.1 Reaction and relaxation time of peri/paraglacial rock slope systems -- 9.4.2 The foreseeable future: transient rock slope systems -- References -- 10 Erosion and sediment flux in mountain watersheds -- 10.1 Introduction -- 10.2 Debris flows and debris floods in high-mountain watersheds -- 10.2.1 Frequency-magnitude relations -- 10.2.2 Climate change and debris-flow activity -- 10.3 Fluvial sediment transport in steep channels -- 10.3.1 Bedload transport calculations in steep streams -- 10.3.2 Limitations of sediment availability -- 10.4 Considerations for sediment-related hazard assessment -- 10.5 Conclusions and outlook -- Acknowledgments -- References -- 11 Glaciers as water resources -- 11.1 Introduction -- 11.2 Regional review of glaciers as water resources -- 11.2.1 The Andes -- 11.2.2 The Swiss Alps -- 11.2.3 The Himalayas -- 11.2.4 Western North America -- 11.3 Summary and future research priorities -- References -- 12 Glacier floods -- 12.1 Introduction -- 12.2 Lake development and outburst processes. , 12.3 Flood form, character and geomorphological impact -- 12.4 Flood modelling and associated challenges -- 12.4.1 Flood magnitude -- 12.4.2 Proglacial flood hydraulic routing/propagation -- 12.4.3 Sediment transport -- 12.5 Identifying hazards and hazard assessment procedures -- 12.6 Managing glacier floods -- 12.7 Summary -- References -- 13 Ecosystem change in high tropical mountains -- 13.1 Introduction -- 13.2 Glacier retreat -- 13.3 Ecological change -- 13.3.1 Primary succession -- 13.3.2 Treeline shifts -- 13.3.3 Shrubland expansion -- 13.3.4 Wetlands and aquatic systems -- 13.4 Land use responses -- 13.5 Conclusions -- Acknowledgments -- References -- Part III Consequences and responses -- 14 The honour of the snow-mountains is the snow: Tibetan livelihoods in a changing climate -- 14.1 Introduction -- 14.2 Hazards and risks as cultural concepts -- 14.2.1 The central Tibetan Plateau: pastoralists coping with snowstorms -- 14.2.1.1 Coping strategies before 1959 -- 14.2.1.2 Changes in coping strategies from the 1950s until present -- 14.2.1.3 Implications for local livelihoods -- 14.2.2 The northern Himalayan slopes: historical perspectives and current challenges -- 14.2.2.1 Porong pastoralists coping with extraordinary snowstorms, sandstorms, and droughts -- 14.2.2.2 Coping with floods -- 14.2.3 The Nepal Himalaya: coping with flood risks to monasteries and livelihoods -- 14.2.3.1 Flood management in historical accounts -- 14.2.3.2 Explanations of the contemporary floods in Halji -- 14.2.3.3 Risk assessment and coping strategies -- 14.3 Conclusion -- Acknowledgements -- References -- 15 Ice-clad volcanoes -- 15.1 Explosive eruptions -- 15.2 Effusive lava eruptions -- 15.3 Pleistocene ice-clad volcanoes -- 15.4 Collapse -- 15.5 Volcano glaciers and climate -- 15.5.1 Recapitulation -- References. , 16 Debris-flow activity from high-elevation, periglacial environments -- 16.1 Introduction -- 16.2 Periglacial debris flows in the Zermatt valley: an overview -- 16.3 Periglacial debris flows in the Zermatt valley: triggers and thresholds -- 16.4 Frequency-magnitude relations of debris flows: mirrors of the state of permafrost? -- 16.5 The future of debris flows in the Zermatt valley: less, unless. . . -- 16.6 Anticipating events without historic precedence -- 16.7 Outlook and conclusions -- References -- 17 Contextualizing conflict: vital waters and competing values in glaciated environments -- 17.1 Introduction -- 17.2 Critical approaches to resource conflicts, scarcity, and governance -- 17.3 Contemporary conflicts in glaciated environments -- 17.3.1 Pascua Lama, Chile -- 17.3.2 Lake Parón, Peru -- 17.3.3 Brahmaputra Basin, China and India -- 17.4 Discussion and conclusion -- Acknowledgments -- References -- Part IV Conclusions -- 18 Synthesis and conclusions: the future of high-mountain cryospheric research -- 18.1 Introduction -- 18.2 Scale -- 18.3 Regional studies -- 18.4 Affected populations and social differentiation -- 18.5 Triggers and drivers -- 18.6 Local knowledge integration -- 18.7 Interdisciplinary teams -- References -- Index.
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  • 2
    Online Resource
    Online Resource
    Berlin, Heidelberg :Springer Berlin / Heidelberg,
    Keywords: Glaciology. ; Electronic books.
    Description / Table of Contents: This is a state-of-the-art interpretive presentation of satellite image data, and analysis of the current state of the world's glaciers. Experts in satellite image analysis of glaciers analyze and interpret the changing nature of glaciers across the globe.
    Type of Medium: Online Resource
    Pages: 1 online resource (936 pages)
    Edition: 1st ed.
    ISBN: 9783540798187
    Series Statement: Springer Praxis Bks.
    DDC: 551.3120223
    Language: English
    Note: Intro -- Contents -- Dedication -- Contributors -- Foreword -- REFERENCES -- Acknowledgments -- Online supplemental material -- Chapter receipt information -- Figures -- Disclaimer: GLIMS is not a border authority -- Tables -- Acronyms and abbreviations -- About the editors -- PROLOGUE Scientific and public perceptions about the importance of fluctuations in glaciers and ice sheets -- P.1 EARLY SCIENTIFIC RECOGNITION OF THE SIGNIFICANCE OF GLACIERS -- P.2 THE PRACTICAL AND PERCEIVED -- P.2 THE PRACTICAL AND PERCEIVEDIMPORTANCE OF GLACIERS TODAY -- P.2.1 Modern understanding of climate change due to greenhouse gases and other causes -- P.2.2 Modern impacts of changing glaciers and ice sheets on people -- P.2.3 Recent public perceptions about -- P.2.4 Time to move on -- P.3 ACKNOWLEDGMENT -- P.4 REFERENCES -- 1 Introduction: Global glacier monitoring-a long-term task integrating in situ observations and remote sensing -- ABSTRACT -- 1.1 WHY THIS BOOK? -- 1.2 PERENNIAL SURFACE ICE ON LAND -- 1.2.1 Definitions -- 1.2.2 Global coverage -- 1.3 GLACIERS AND CLIMATE -- 1.3.1 Formation of glaciers and their dynamical controls -- 1.3.2 Glacier reactions to climate change, -- 1.3.3 Reporting glacier change rates -- 1.3.3 Reporting glacier change rates -- 1.4 INTERNATIONAL GLACIER MONITORING -- 1.4.1 History of international glacier monitoring in the 19th and 20th centuries -- 1.4.2 The Global Terrestrial Network for -- 1.4.2 The Global Terrestrial Network for Glaciers (GTN-G) -- 1.4.3 Available datasets -- 1.4.4 Challenges of the 21st century -- 1.5 GLACIER OBSERVATIONS FROM SPACE -- 1.5.1 Satellite observations in GTN-G -- 1.5.2 Possible applications -- 1.5.3 Challenges -- 1.7 SYNOPSIS AND ORGANIZATION OF THE BOOK -- 1.6 INTEGRATIVE GLACIER CHANGE ASSESSMENTS -- 1.8 CONCLUSIONS -- 1.9 ACKNOWLEDGMENTS -- 1.10 REFERENCES. , 2 Theoretical foundations of remote sensing for glacier assessment and mapping -- ABSTRACT -- 2.1 INTRODUCTION -- 2.2 RADIATION TRANSFER CASCADE -- 2.2.1 Solar irradiance -- 2.2.2 Surface irradiance -- 2.2.3 Surface reflectance -- 2.2.4 Surface emission -- 2.3 SURFACE-ENERGY INTERACTIONS -- 2.3.1 Snow -- 2.3.2 Glaciers -- 2.3.3 Water -- 2.4 COMPLICATIONS -- 2.5 SPACE-BASED INFORMATION EXTRACTION -- 2.5.1 Snow cover -- 2.5.2 Ice sheets 2.5.3 Alpine glacier mapping -- 2.5.4 Debris-covered glaciers -- 2.5.5 Snow line and ELA -- 2.5.6 Ice flow velocities -- 2.6 NUMERICAL MODELING -- 2.6.1 Climate modeling -- 2.6.2 Energy balance modeling -- 2.6.3 Glacier mass balance modeling -- 2.7 CONCLUSIONS -- 2.8 ACKNOWLEDGMENTS -- 2.9 NOTATION -- 2.10 REFERENCES -- 3 Radiative transfer modeling in the cryosphere -- ABSTRACT -- 3.1 INTRODUCTION -- 3.2 RADIATIVE TRANSFER MODELING OF GLACIER SURFACES -- 3.2.1 RT modeling approach for glacier surfaces -- 3.2.2 Radiative transfer equation inlayered mixtures of snow, ice, and debris -- 3.2.3 Radiative transfer equation in glacier lake waters -- 3.3 OPTICAL PROPERTIES OF SNOW,ICE, DEBRIS, MIXTURES, AND GLACIER LAKE WATER -- 3.3.1 Snow -- 3.3.2 Glacier ice -- 3.3.3 Rock debris -- 3.3.4 Mixtures -- 3.3.5 Glacier lake water -- 3.4 NUMERICAL SOLUTION OF THE RTE -- 3.5 GLACIER RADIATIVE TRANSFER -- 3.5 GLACIER RADIATIVE TRANSFER SIMULATION EXAMPLES -- 3.6 CONCLUSIONS -- 3.7 REFERENCES -- 4 Glacier mapping and monitoring using multispectral data -- ABSTRACT -- 4.1 INTRODUCTION -- 4.2 IMAGE PREPROCESSING -- 4.2.1 Radiometric calibration -- 4.2.2 Geometric preprocessing -- 4.3 MULTISPECTRAL METHODS -- 4.3.1 Spectral reflectance of glacier surfaces -- 4.3.2 Image classification approaches -- 4.3.3 Image-processing techniques -- 4.3.4 Postprocessing and GIS work flow -- 4.4 MAPPING DEBRIS-COVERED ICE -- 4.5 THERMAL IMAGING. , 4.6 MICROWAVE/SAR METHODS -- 4.7 SPECTRAL CHANGE DETECTION AND TEMPORAL DATA MERGING -- 4.7.1 Overview -- 4.7.2 Image change evaluation by subtraction of multispectral anniversary pairs (ICESMAP) -- 4.8 ICE FLOW -- 4.8.1 Image choice and preprocessing for image matching -- 4.8.2 Image-matching techniques -- 4.8.3 Postprocessing and analysis -- 4.8.4 Accuracy -- 4.8.5 SAR offset tracking and interferometry -- 4.9 CHALLENGES, CONCLUSIONS, AND PERSPECTIVES -- 4.10 ACKNOWLEDGMENTS -- 4.11 REFERENCES -- 5 Digital terrain modeling and glacier topographic characterization -- ABSTRACT -- 5.1 INTRODUCTION -- 5.2 BACKGROUND -- 5.3 DIGITAL ELEVATION MODEL GENERATION -- 5.3.1 Source data -- 5.3.2 Aerial and satellite image stereoscopy -- 5.3.3 Ground control points -- 5.3.5 Postprocessing (interpolation and smoothing) -- 5.3.6 Data fusion -- 5.4 DEM ERROR AND UNCERTAINTY -- 5.4.1 Representation of DEM error and uncertainty -- 5.4.2 Type and origin of errors -- 5.5 GEOMORPHOMETRY -- 5.5.1 Geomorphometric land surface parameters -- 5.5.2 Scale-dependent analysis -- 5.5.3 Topographic radiation modeling -- 5.5.4 Altitude functions -- 5.5.5 Glacier elevation changes and mass balance calculations -- 5.6 GLACIER MAPPING -- 5.6.1 Pattern recognition -- 5.6.2 Artificial intelligence techniques -- 5.6.3 Object-oriented mapping -- 5.7 DISCUSSION -- 5.9 ACKNOWLEDGMENTS -- 5.8 CONCLUSIONS -- 5.10 REFERENCES -- 6 ASTER datasets and derived products for global glacier monitoring -- ABSTRACT -- 6.1 INTRODUCTION -- 6.2 ASTER DATA ACCESS AND USE POLICY -- 6.3 ASTER DATA -- 6.3.1 Performance of ASTER VNIR, SWIR, and TIR -- 6.4 ASTER DATA-PROCESSING STREAM -- 6.4.1 Standard Level 1A and Level 1B -- 6.4.2 ASTER standard higher level products -- 6.5 ASTER DATA FOR GLIMS: STARS, DARs, GAIN SETTINGS, AND IMAGE SEASONS -- 6.6 ACKNOWLEDGMENTS -- 6.7 REFERENCES. , 7 Quality in the GLIMS Glacier Database -- ABSTRACT -- 7.1 INTRODUCTION -- 7.2 STANDARD METHODS AND TOOLS -- 7.3 ACCURACY AND PRECISION IN GLACIER MAPPING -- 7.4 GLACIER ANALYSIS COMPARISON EXPERIMENTS (GLACE) -- 7.4.1 GLACE 1 and GLACE 2 -- 7.4.2 GLACE 2A and GLACE 3A (manual digitization) -- 7.5 GLACE RESULTS -- 7.5.1 GLACE 1 and GLACE 2 -- 7.5.2 GLACE 2A and GLACE 3A -- 7.5.3 Discussion -- 7.6 GLIMS GLACIER DATABASE AND THE DATA INGEST PROCESS -- 7.6.1 Ingest quality control steps -- 7.6.2 Representation of measurement error -- 7.6.3 Derived parameters in the database -- 7.7 CONCLUSION -- 7.8 ACKNOWLEDGMENTS -- 7.9 REFERENCES -- 8 Glacier fluctuations and dynamics around the margin of the Greenland Ice Sheet -- ABSTRACT -- 8.1 GREENLAND GLACIOLOGY -- 8.1.1 Ice sheet mass changes -- 8.2 CASE STUDY 1: CENTRAL EAST GREENLAND MARGIN FLUCTUATIONS AND CLIMATESENSITIVITY FROM A GLIMS GLACIER INVENTORY AND ASTER GDEM -- 8.2.1 Introduction -- 8.2.2 Methods -- 8.2.3 Results -- 8.3 CASE STUDY 2: A COMPARISON OF HIGH-RATE GPS AND ASTERDERIVED MEASUREMENTS ON HELHEIM GLACIER -- 8.3.1 Introduction -- 8.3.2 Data -- 8.3.3 Results -- 8.4 DISCUSSION AND CONCLUSION -- 8.5 ACKNOWLEDGMENTS -- 8.6 REFERENCES -- 9 Remote sensing of recent glacier changes in the Canadian Arctic -- ABSTRACT -- 9.1 INTRODUCTION -- 9.2 REGIONAL CONTEXT -- 9.2.1 Geology and physiography -- 9.2.2 Climate and recent climate trends in the Canadian Arctic -- 9.2.3 Glacier characteristics -- 9.3 SPECIAL TOPICS: REGIONAL GLACIER MASS BALANCE AND PROXY INDICATORS -- 9.3.1 Surface mass balance and mass balance changes -- 9.3.2 Summer melt -- 9.3.3 Ice flow and iceberg-calving fluxes -- 9.4 CASE STUDIES -- 9.4.1 Surge-type glaciers -- 9.4.2 Northern Ellesmere Island ice shelves -- 9.5 REGIONAL SYNTHESIS: RECENT CHANGES IN EQUILIBRIUM LINE ALTITUDE AND GLACIER EXTENT -- 9.5.1 Methodology. , 9.5.2 Results -- 9.6 KEY ISSUE -- 9.6.1 Changes in glacier surface elevation, volume, and mass -- sealevel contributions -- 9.7 SUMMARY AND CONCLUSIONS -- 9.8 ACKNOWLEDGMENTS -- 9.9 REFERENCES -- 10 A digital glacier database for Svalbard -- ABSTRACT -- 10.1 INTRODUCTION -- 10.2 REGIONAL CONTEXT -- 10.3 DATABASE STRUCTURE -- 10.4 DATA -- 10.4.1 The original Topographic Map Series of Svalbard (S100)-1936/1966/1971 -- 10.4.2 The 1990 photogrammetric survey -- 10.4.3 The satellite dataset -- 10.5 METHODOLOGY -- 10.5.1 Creation of glacier outlines from cartographic data for the 1936/1966/1971 dataset -- 10.5.2 Creation of outlines from cartographic data for the 1990 dataset -- 10.5.3 Creation of outlines from satellite data for the 2001-2010 dataset -- 10.5.4 Glacier and snow patches smaller than 1 km2 -- 10.6 RESULTS -- 10.7 CONCLUSIONS AND FUTURE PERSPECTIVES -- 10.9 REFERENCES -- 10.8 ACKNOWLEDGMENTS -- 11 Alaska: Glaciers of Kenai Fjords National Park and Katmai National Park and Preserve -- ABSTRACT -- 11.1 INTRODUCTION -- 11.2 REGIONAL CONTEXT -- 11.2.1 Geographic/topographic/environmental setting -- 11.2.2 Climate -- 11.2.3 Glacier characteristics-Kenai -- 11.2.4 Glacier characteristics-Katmai -- 11.2.3 Glacier characteristics-Kenai Fjords National Park -- 11.3 PROCEDURES FOR ANALYSIS OF GLACIER CHANGES -- 11.3.1 Imagery classification -- 11.3.3 Manual editing -- 11.3.2 Complicating issues -- 11.4 SATELLITE IMAGERY INTERPRETATION ACCURACY -- 11.5 AREAL EXTENT-GLACIER ICE -- 11.5.1 Kenai Fjords National Park -- 11.5.2 Katmai National Park and Preserve -- 11.6 TERMINUS POSITION MEASUREMENTS -- 11.6.1 Methodology -- 11.6.2 Kenai Fjords National Park -- 11.6.3 Katmai National Park and Preserve -- 11.7 DISCUSSION AND CONCLUSIONS -- 11.8 REFERENCES -- 12 Glacier-dammed ice-marginal lakes of Alaska -- ABSTRACT -- 12.1 INTRODUCTION. , 12.2 REGIONAL CONTEXT.
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  • 3
    Publication Date: 2023-03-16
    Description: In permafrost areas, seasonal freeze-thaw cycles of active layer result in upward and downward movements of the ground. Additionally, relatively uniform thawing of the ice-rich layer at the permafrost table can contribute to net long-term surface lowering. We use a simple method to quantify surface lowering (subsidence) and uplift in a yedoma area of the Lena River Delta, Siberian Arctic (Kurungnakh Island), using reference rods (metal pipes and fiberglass rods) installed deeply in permafrost. The metal pipes were 2 m long and 3 cm in diameter and were anchored at least 1 m below the typical active layer. The fiberglass rods were 2 m long and 1 cm in diameter and were anchored at least 70 m below the typical active layer. We assume, therefore, that the rods were motionless relative to the permafrost. The plexiglass plate with a size of 10 by 10 cm was fixed in its horizontal position by the rod but could move freely with the surface vertically along the rod. We repeatedly measured distance between the top of a rod and a plexiglass plate resting on the ground surface. Several distance measurements around each rod were taken at each visit and averaged. Altogether 12 metal pipes were installed at the study site in April 2013 and 19 fiberglass rods were installed in April 2014. Measurements were conducted during field campaigns from spring 2013 to summer 2017 with some gaps. We provide here the measured distances between the top of a rod and a plexiglass plate. To obtain the ground displacement, the user have to define the period of interest and calculate the displacement.
    Keywords: 10; 11; 12; 13; 14; 15; 16; 7; 8; 9; AWI_Envi; AWI_PerDyn; AWI_Perma; DATE/TIME; DISTANCE; Event label; Kurungnakh_10; Kurungnakh_11; Kurungnakh_12; Kurungnakh_13; Kurungnakh_14; Kurungnakh_15; Kurungnakh_16; Kurungnakh_7; Kurungnakh_8; Kurungnakh_9; Kurungnakh Island, Lena Delta, Siberia; LAND; Permafrost Research; Permafrost Research (Periglacial Dynamics) @ AWI; Polar Terrestrial Environmental Systems @ AWI; Sampling/measurement on land; Station label
    Type: Dataset
    Format: text/tab-separated-values, 111 data points
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  • 4
    Publication Date: 2023-03-16
    Description: In permafrost areas, seasonal freeze-thaw cycles of active layer result in upward and downward movements of the ground. Additionally, relatively uniform thawing of the ice-rich layer at the permafrost table can contribute to net long-term surface lowering. We use a simple method to quantify surface lowering (subsidence) and uplift in a yedoma area of the Lena River Delta, Siberian Arctic (Kurungnakh Island), using reference rods (metal pipes and fiberglass rods) installed deeply in permafrost. The metal pipes were 2 m long and 3 cm in diameter and were anchored at least 1 m below the typical active layer. The fiberglass rods were 2 m long and 1 cm in diameter and were anchored at least 70 m below the typical active layer. We assume, therefore, that the rods were motionless relative to the permafrost. The plexiglass plate with a size of 10 by 10 cm was fixed in its horizontal position by the rod but could move freely with the surface vertically along the rod. We repeatedly measured distance between the top of a rod and a plexiglass plate resting on the ground surface. Several distance measurements around each rod were taken at each visit and averaged. Altogether 12 metal pipes were installed at the study site in April 2013 and 19 fiberglass rods were installed in April 2014. Measurements were conducted during field campaigns from spring 2013 to summer 2017 with some gaps. We provide here the measured distances between the top of a rod and a plexiglass plate. To obtain the ground displacement, the user have to define the period of interest and calculate the displacement.
    Keywords: 4; 5; 6; 7; 8; 9; AWI_Envi; AWI_PerDyn; AWI_Perma; DATE/TIME; DISTANCE; Event label; Kurungnakh_4; Kurungnakh_5; Kurungnakh_6; Kurungnakh_7; Kurungnakh_8; Kurungnakh_9; Kurungnakh_mid_1; Kurungnakh_mid_2; Kurungnakh_north_1; Kurungnakh_north_2; Kurungnakh_south_1; Kurungnakh_south_2; Kurungnakh Island, Lena Delta, Siberia; LAND; mid_1; mid_2; north_1; north_2; Permafrost Research; Permafrost Research (Periglacial Dynamics) @ AWI; Polar Terrestrial Environmental Systems @ AWI; Sampling/measurement on land; south_1; south_2; Station label
    Type: Dataset
    Format: text/tab-separated-values, 118 data points
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  • 5
    Publication Date: 2023-03-16
    Description: Differential SAR interferometry (DInSAR) uses the phase difference between two SAR signals acquired on two dates over the same area to measure small-scale ground motion. During the last decade the method has been adapted for monitoring permafrost-related ground motion. Here we perform DInSAR on TerraSAR-X data to assess its viability for seasonal thaw subsidence detection in a yedoma landscape of the Lena River Delta. TerraSAR-X is a right-looking SAR satellite launched in 2007, operating in the X-band (wavelength 3.1 cm, frequency 9.6 GHz), with a revisit time of eleven days. All data that we used were acquired in StripMap mode with HH polarization from a descending orbit at 08:34 local acquisition time (22:34 UTC). The incidence angle of the track we use is approximately 31 degrees. The scene size covered an area of approximately 18 km x 56 km. The slant range and azimuth pixel spacing were approximately 0.9 m and 2.4 m, respectively. Based on the ground temperature data we roughly estimated the beginning and the end of thaw season in 2013. The corresponding TerraSAR-X time series used for this study includes nine Single-Look Slant Range Complex (SSC) images taken between 7 June and 14 September 2013. The time span between the acquisitions that we used for interferometry was 11 days, with one exception when the time span was 22 days due to a missing acquisition. The data were processed using the Gamma radar software. The SSC data were converted to Gamma Single Look Complex (SLC) format and the SLC data were then consecutively co-registered with subpixel accuracy (typically better than 0.2 pixels) in such a way that the co-registered slave image became the master for the next image. This way of co-registering also ensures subpixel co-registration accuracy for all interferometric combinations of the nine images. Multilooking was performed with the factor 4 in the range and factor 3 in the azimuth directions to reduce the noise and obtain roughly square ground range pixels. The ground size of the multilooked pixel is approximately 7 m. We removed the topographic phase term using ArcticDEM that is a freely available high-resolution (5 m) circum-Arctic DEM produced from optical stereographic WorldView imagery acquired from 2012–2016. Obtained differential interferograms were then filtered with an adaptive filter based on the local fringe spectrum with the filtering window size of 128 pixels and an alpha exponent of 0.4. Interferograms, featuring especially low coherence, were additionally filtered with a window size of 64 pixels. For the phase unwrapping we used a branch-cut algorithm with the seeding point located approximately in the middle of the study area with relatively high coherence. We did not attempt to unwrap the areas, separated from the main study area by the river channels. The influence of atmospheric phase delays was evident in the unwarpped interferograms. In order to enhance the displacement signal and reduce atmospheric noise, all eight unwrapped interferograms were summed up in a time-continuous stack. Phase rate per day was calculated from the stack. A strong linear ramp was present across the phase rate map. To remove the trend, a 2D linear function was fit to the data and then subtracted from the phase rate map. The phase rate was then converted to vertical displacement rate in meters, under the assumption that the ground movement is purely vertical. The resulting displacement rate map was geocoded using ArcticDEM to the Universal Transverse Mercator (UTM) projection, zone 52N WGS84 with a pixel size of 5 m. The map was finally converted to the displacement magnitude by multiplying the rate by 99 days (from 7 June to 14 September 2013) and converted to centimeters. As opposed to the results, published in the related paper, here we did not start the unwrapping from the known bedrock position, as it was partly affected by low coherence as well as rather remote from the main area of interest and only weakly connected to the rest of the map over a small and noisy area of valid pixels. It means that the displacement map published here, features only displacement values relative to each other, without a fixed reference point. The spatial pattern of the signal, however, did not change with this alteration in processing. The DInSAR map showed a distinct subsidence in most of the thermokarst basins relative to the upland. Moreover, the spatial pattern of DInSAR signal was in high agreement with the surface wetness in the basins, identified with the near infra-red band of a high-resolution optical image. Drier parts of the basins were clearly separated from wetter parts that showed a prominent subsidence. In general, low coherence in combination with atmospheric effects as well as remoteness of a reference ground point were severe obstacles for the retrieval of a wide-area seasonal thaw subsidence map with TerraSAR-X data.
    Keywords: AWI_Envi; AWI_PerDyn; AWI_Perma; AWI Arctic Land Expedition; Kurungnakh_Island; Lena2013; Permafrost Research; Permafrost Research (Periglacial Dynamics) @ AWI; Polar Terrestrial Environmental Systems @ AWI; RU-Land_2013_Lena; SAT; Satellite remote sensing
    Type: Dataset
    Format: image/tiff, 337.2 MBytes
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  • 6
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    In:  Supplement to: Antonova, Sofia; Sudhaus, Henriette; Strozzi, Tazio; Zwieback, Simon; Kääb, Andreas; Heim, Birgit; Langer, Moritz; Bornemann, Niko; Boike, Julia (2018): Thaw subsidence of a yedoma landscape in Northern Siberia, measured in situ and estimated from TerraSAR-X interferometry. Remote Sensing, 10(4), 494, https://doi.org/10.3390/rs10040494
    Publication Date: 2023-03-16
    Description: In permafrost areas, seasonal freeze-thaw cycles result in upward and downward movements of the ground. For some permafrost areas, long-term downward movements were reported during the last decade. We measured seasonal and multi-year ground movements in a yedoma region of the Lena River Delta, Siberia, in 2013–2017, using reference rods installed deep in the permafrost. The seasonal subsidence was 1.7 ± 1.5 cm in the cold summer of 2013 and 4.8 ± 2 cm in the warm summer of 2014. Furthermore, we measured a pronounced multi-year net subsidence of 9.3 ± 5.7 cm from spring 2013 to the end of summer 2017. Importantly, we observed a high spatial variability of subsidence of up to 6 cm across a sub-meter horizontal scale. In summer 2013, we accompanied our field measurements with Differential Synthetic Aperture Radar Interferometry (DInSAR) on repeat-pass TerraSAR-X (TSX) data from the summer of 2013 to detect summer thaw subsidence over the same study area. Interferometry was strongly affected by a fast phase coherence loss, atmospheric artifacts, and possibly the choice of reference point. A cumulative ground movement map, built from a continuous interferogram stack, did not reveal a subsidence on the upland but showed a distinct subsidence of up to 2 cm in most of the thermokarst basins. There, the spatial pattern of DInSAR-measured subsidence corresponded well with relative surface wetness identified with the near infra-red band of a high-resolution optical image. Our study suggests that (i) although X-band SAR has serious limitations for ground movement monitoring in permafrost landscapes, it can provide valuable information for specific environments like thermokarst basins, and (ii) due to the high sub-pixel spatial variability of ground movements, a validation scheme needs to be developed and implemented for future DInSAR studies in permafrost environments.
    Keywords: AWI_Envi; AWI_PerDyn; AWI_Perma; Permafrost Research; Permafrost Research (Periglacial Dynamics) @ AWI; Polar Terrestrial Environmental Systems @ AWI
    Type: Dataset
    Format: application/zip, 3 datasets
    Location Call Number Limitation Availability
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  • 7
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    Unknown
    PANGAEA
    In:  Supplement to: Antonova, Sofia; Duguay, Claude R; Kääb, Andreas; Heim, Birgit; Langer, Moritz; Westermann, Sebastian; Boike, Julia (2016): Monitoring bedfast ice and ice phenology in lakes of the Lena River Delta using TerraSAR-X backscatter and coherence time series. Remote Sensing, 8(11), 903, https://doi.org/10.3390/rs8110903
    Publication Date: 2023-05-12
    Description: Thermokarst lakes and ponds are major elements of permafrost landscapes, occupying up to 40% of the land area in some Arctic regions. Shallow lakes freeze to the bed, thus preventing permafrost thaw underneath them and limiting the length of the period with greenhouse gas production in the unfrozen lake sediments. Radar remote sensing permits to distinguish lakes with bedfast ice due to the difference in backscatter intensities from bedfast and floating ice. This study investigates the potential of a unique time series of three-year repeat-pass TerraSAR-X (TSX) imagery with high temporal (11 days) and spatial (10 m) resolution for monitoring bedfast ice as well as ice phenology of lakes in the zone of continuous permafrost in the Lena River Delta, Siberia. TSX backscatter intensity is shown to be an excellent tool for monitoring floating versus bedfast lake ice as well as ice phenology. TSX-derived timing of ice grounding and the ice growth model CLIMo are used to retrieve the ice thicknesses of the bedfast ice at points where in situ ice thickness measurements were available. Comparison shows good agreement in the year of field measurements. Additionally, for the first time, an 11-day sequential interferometric coherence time series is analyzed as a supplementary approach for the bedfast ice monitoring. The coherence time series detects most of the ice grounding as well as spring snow/ice melt onset. Overall, the results show the great value of TSX time series for monitoring Arctic lake ice and provide a basis for various applications: for instance, derivation of shallow lakes bathymetry, evaluation of winter water resources and locating fish winter habitat as well as estimation of taliks extent in permafrost.
    Type: Dataset
    Format: application/zip, 2 datasets
    Location Call Number Limitation Availability
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  • 8
    facet.materialart.
    Unknown
    PANGAEA
    In:  Supplement to: Antonova, Sofia; Kääb, Andreas; Heim, Birgit; Langer, Moritz; Boike, Julia (2016): Spatio-temporal variability of X-band radar backscatter and coherence over the Lena River Delta, Siberia. Remote Sensing of Environment, 182, 169-191, https://doi.org/10.1016/j.rse.2016.05.003
    Publication Date: 2023-05-12
    Description: Satellite-based monitoring strategies for permafrost remain under development and are not yet operational. Remote sensing allows indirect observation of permafrost, a subsurface phenomenon, by mapping surface features or measuring physical parameters that can be used for permafrost modeling. We have explored high temporal resolution time series of TerraSAR-X backscatter intensity and interferometric coherence for the period between August 2012 and September 2013 to assess their potential for detecting major seasonal changes to the land surface in a variety of tundra environments within the Lena River Delta, Siberia. The TerraSAR-X signal is believed to be strongly affected by the vegetation layer, and its viability for the retrieval of soil moisture, for example, is therefore limited. In our study individual events, such as rain and snow showers, that occurred at the time of TerraSAR-X acquisition, or a refrozen crust on the snowpack during the spring melt were detected based on backscatter intensity signatures. The interferometric coherence showed marked variability; the snow cover onset and snow melt periods were identified by significant reduction in coherence. Principal component analysis provided a good spatial overview of the essential information contained in backscatter and coherence time series and revealed latent relationships between both time series and the surface temperature. The results of these investigations suggest that although X-band SAR has limitations with respect to monitoring seasonal land surface changes in permafrost areas, high-resolution time series of TerraSAR-X backscatter and coherence can provide new insights into environmental conditions.
    Keywords: AWI_Envi; AWI_Perma; Permafrost Research; Polar Terrestrial Environmental Systems @ AWI
    Type: Dataset
    Format: application/zip, 2 datasets
    Location Call Number Limitation Availability
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  • 9
    facet.materialart.
    Unknown
    PANGAEA
    In:  Supplement to: Brun, Fanny; Berthier, Etienne; Wagnon, Patrick; Kääb, Andreas; Treichler, Désirée (2017): A spatially resolved estimate of High Mountain Asia glacier mass balances from 2000 to 2016. Nature Geoscience, 10(9), 668-673, https://doi.org/10.1038/ngeo2999
    Publication Date: 2023-01-13
    Description: High Mountain Asia hosts the largest glacier concentration outside the polar regions. These glaciers are important contributors to streamflow in one of the most populated areas of the world. Past studies have used methods that can provide only regionally averaged glacier mass balances to assess the glacier contribution to rivers and sea level rise. Here we compute the mass balance for about 92% of the glacierized area of High Mountain Asia using time series of digital elevation models derived from satellite stereo-imagery. We calculate a total mass change of -16.3 ± 3.5Gt/yr (-0.18 ± 0.04 m w.e./yr) between 2000 and 2016, which is less negative than most previous estimates. Region-wide mass balances vary from -4.0 ± 1.5 Gt/yr (-0.62 ± 0.23 m w.e./yr) in Nyainqentanglha to +1.4 ± 0.8 Gt/yr (+0.14 ± 0.08 m w.e./yr) in Kunlun, with large intra-regional variability of individual glacier mass balances (standard deviation within a region ~0.20 m w.e./yr). Specifically, our results shed light on the Nyainqentanglha and Pamir glacier mass changes, for which contradictory estimates exist in the literature. They provide crucial information for the calibration of the models used for projecting glacier response to climatic change, as these models do not capture the pattern, magnitude and intra-regional variability of glacier changes at present.
    Keywords: ASTER_n27_e086; ASTER_n27_e087; ASTER_n27_e088; ASTER_n27_e092; ASTER_n28_e083; ASTER_n28_e084; ASTER_n28_e085; ASTER_n28_e086; ASTER_n28_e087; ASTER_n28_e089; ASTER_n28_e090; ASTER_n28_e091; ASTER_n28_e092; ASTER_n28_e097; ASTER_n28_e098; ASTER_n29_e081; ASTER_n29_e082; ASTER_n29_e083; ASTER_n29_e094; ASTER_n29_e095; ASTER_n29_e096; ASTER_n29_e097; ASTER_n29_e101; ASTER_n30_e078; ASTER_n30_e079; ASTER_n30_e080; ASTER_n30_e081; ASTER_n30_e082; ASTER_n30_e083; ASTER_n30_e090; ASTER_n30_e093; ASTER_n30_e094; ASTER_n30_e095; ASTER_n31_e077; ASTER_n31_e078; ASTER_n31_e079; ASTER_n31_e083; ASTER_n31_e094; ASTER_n32_e076; ASTER_n32_e077; ASTER_n32_e078; ASTER_n32_e092; ASTER_n33_e075; ASTER_n33_e076; ASTER_n33_e077; ASTER_n33_e078; ASTER_n33_e079; ASTER_n33_e082; ASTER_n33_e089; ASTER_n33_e090; ASTER_n33_e091; ASTER_n33_e094; ASTER_n34_e075; ASTER_n34_e076; ASTER_n34_e077; ASTER_n34_e078; ASTER_n34_e079; ASTER_n34_e080; ASTER_n34_e081; ASTER_n34_e082; ASTER_n34_e085; ASTER_n35_e070; ASTER_n35_e072; ASTER_n35_e073; ASTER_n35_e074; ASTER_n35_e075; ASTER_n35_e076; ASTER_n35_e077; ASTER_n35_e078; ASTER_n35_e079; ASTER_n35_e080; ASTER_n35_e081; ASTER_n35_e082; ASTER_n35_e089; ASTER_n35_e090; ASTER_n36_e070; ASTER_n36_e071; ASTER_n36_e072; ASTER_n36_e073; ASTER_n36_e074; ASTER_n36_e075; ASTER_n36_e076; ASTER_n36_e077; ASTER_n36_e078; ASTER_n36_e079; ASTER_n36_e082; ASTER_n36_e084; ASTER_n36_e087; ASTER_n36_e090; ASTER_n36_e091; ASTER_n37_e071; ASTER_n37_e072; ASTER_n37_e073; ASTER_n37_e074; ASTER_n37_e075; ASTER_n37_e087; ASTER_n38_e071; ASTER_n38_e072; ASTER_n38_e073; ASTER_n38_e075; ASTER_n38_e096; ASTER_n38_e097; ASTER_n39_e069; ASTER_n39_e070; ASTER_n39_e071; ASTER_n39_e072; ASTER_n39_e073; ASTER_n39_e074; ASTER_n39_e098; ASTER_n40_e074; ASTER_n41_e076; ASTER_n41_e077; ASTER_n41_e078; ASTER_n41_e079; ASTER_n41_e080; ASTER_n42_e074; ASTER_n42_e077; ASTER_n42_e078; ASTER_n42_e079; ASTER_n42_e080; ASTER_n42_e081; ASTER_n42_e082; ASTER_n42_e085; ASTER_n43_e077; ASTER_n43_e083; ASTER_n43_e084; ASTER_n43_e085; ASTER_n43_e086; ASTER_n44_e079; ASTER_n44_e080; ASTER_n44_e083; ASTER_n45_e080; DATE/TIME; Event label; File name; File size; High Mountain Asia; SAT; Satellite remote sensing; Uniform resource locator/link to file
    Type: Dataset
    Format: text/tab-separated-values, 792 data points
    Location Call Number Limitation Availability
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  • 10
    Publication Date: 2023-05-12
    Description: The goal of this study was to examine the potential of a unique X-band SAR dataset to monitor ice phenology and bedfast ice on a number of thermokarst lakes in the Siberian Arctic. Three-year repeat-pass TSX time series with high temporal (11 days) and spatial (10 m) resolution were used. Two different parameters derived from SAR imagery were employed in the analysis: backscatter intensity and 11-day interferometric coherence. In situ ice thickness measurements were collected at 14 locations from a sample of 10 lakes in April 2015. A region of interest (ROI) was created around each in situ ice thickness measurement location as a circle with a diameter of approximately 10 pixels. We provide extracted backscatter and coherence for all the ROIs as georeferenced .tif files for the entire time series.
    Keywords: AWI Arctic Land Expedition; File format; File name; File size; Kurungnakh_Island; Lena2013; RU-Land_2013_Lena; SAT; Satellite remote sensing; Uniform resource locator/link to file
    Type: Dataset
    Format: text/tab-separated-values, 12 data points
    Location Call Number Limitation Availability
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