The maps in this data release show active landslide structures in three areas along the north flank of the Slumgullion landslide. After the entire active part of the landslide was mapped in 1992 and 1993 (Fleming and others, 1999), we remapped these three smaller areas at roughly decadal intervals. Our goal was to learn what structures might persist and how they might change as heterogeneous landslide material of variable thickness passed through the areas. Together with the original 1999 map, these maps provide snapshots of the deformational features at converging and diverging margins of the landslide at four periods in about a 30-year time span (1992-2023). During summer months in 2002, 2013, and 2023, we conducted 1:1000-scale mapping using a traditional technique of manually drawing lines on topographic base maps to represent the structures we observed in the field. There was generally a lapse of two or more years between acquisition of the topographic base data and the field mapping. Meters of landslide displacement during the lapse resulted in a mismatch between the topographic map and topography on the active landslide at the time of our fieldwork. When drawing features on the topographic base, we referenced fixed topographic features directly north of the active landslide’s strike-slip boundary to compensate for the mismatch. The data are recorded in Geographic Information System (GIS) files that contain the line styles used to portray and distinguish the different landslide structures. The files record the shapes and positions of the mapped landslide structures. An index of line styles used to portray mapped structures is shown in Figure 1. Topographic base maps used for the 2002, 2013, and 2023 structural maps were from 2000, 2011, and 2018, respectively. One-meter Digital Elevation Models (DEMs), contours, and shaded-relief maps from these three years are included in this data release. The 2000 DEM was created from 2 m contours of the landslide on July 31, 2000, as originally published in Messerich and Coe (2003). The 2011 DEM was created by the authors using a structure-from-motion photogrammetric method and 1:6000 scale aerial photos acquired on September 23, 2011. The 2018 DEM is lidar data collected between October 5, 2018 and September 24, 2019, with the original data available from the U.S. Geological Survey 3DEP Lidar Explorer (U.S. Geological Survey, 2024). The contour interval used for the 2000 DEM is 2 m. The contour interval used for the 2011 and 2018 DEM is 1 m. All GIS data are projected in the Universal Transverse Mercator (UTM) zone 13N cartesian coordinate system. Portable Document Format (PDF) files of the landslide structure maps of each area in 2002, 2013, and 2023, are also provided. Figure 1. Line and polygon types used for landslide structures and features mapped at the Slumgullion landslide. References Fleming, R.W., Baum, R.L., and Giardino, Marco, 1999, Map and description of the active part of the Slumgullion Landslide, Hinsdale County, Colorado: U.S. Geological Survey Geologic Investigations Series Map I-2672 , scale 1:1,000, https://doi.org/10.3133/i2672 Messerich, J.A. and Coe, J.A., 2003, Topographic map of the active part of the Slumgullion landslide on July 31, 2000, Hinsdale County, Colorado: U.S. Geological Survey Open-File Report 03-144, 7 p., 1:1,000 scale map. http://pubs.usgs.gov/of/2003/ofr-03-144/ U.S. Geological Survey, 2024, 3DEP Lidar Explorer, data available at: http://prd-tnm.s3.amazonaws.com/index.html?prefix=StagedProducts/Elevation/1m/Projects/CO_Southwest_NRCS_2018_D18

The winter rainy season of 2016-2017 brought abundant rainfall to the state of California, including the San Francisco Bay region. Thousands of shallow landslides were triggered as a result of saturated soils and intense rainfall from strong winter storms in January and February 2017. The highest concentration of landslides from these storms occurred in the eastern part of the bay region, where landslides in the hills east of the Cities of Richmond, Berkeley, Oakland, Hayward, and Fremont, and elsewhere in the region, damaged homes, displaced a major electrical transmission-line tower, and blocked several heavily traveled state highway routes. The data presented here support our published map titled, "Landslides Triggered by the 2016-2017 Storm Season, Eastern San Francisco Bay Region, California" where we mapped a total of 8,928 landslides throughout the study area. The mapping encompasses a total area of approximately 1,050 square kilometers (km²) bounded by the Carquinez Strait and San Francisco Bay to the north and west, respectively, to the Interstate Highway 680 corridor to the south and east. Using high-resolution imagery, we mapped individual landslides as polygons. The greatest calculated landslide concentration (measured as the total number of landslides per unit area) exceeded 80 landslides per 0.25 km2 in the hills east of the City of Berkeley.

The winter rainy season of 2016-2017 brought abundant rainfall to the state of California, including the San Francisco Bay region. Thousands of shallow landslides were triggered as a result of saturated soils and intense rainfall from strong winter storms in January and February 2017. The highest concentration of landslides from these storms occurred in the eastern part of the bay region, where landslides in the hills east of the Cities of Richmond, Berkeley, Oakland, Hayward, and Fremont, and elsewhere in the region, damaged homes, displaced a major electrical transmission-line tower, and blocked several heavily traveled state highway routes. The data presented here support our published map titled, "Landslides Triggered by the 2016-2017 Storm Season, Eastern San Francisco Bay Region, California" where we mapped a total of 8,928 landslides throughout the study area. The mapping encompasses a total area of approximately 1,050 square kilometers (km²) bounded by the Carquinez Strait and San Francisco Bay to the north and west, respectively, to the Interstate Highway 680 corridor to the south and east. Using high-resolution imagery, we mapped individual landslides as polygons. The greatest calculated landslide concentration (measured as the total number of landslides per unit area) exceeded 80 landslides per 0.25 km2 in the hills east of the City of Berkeley.

Two active landslides at and near the retreating front of Barry Glacier at the head of Barry Arm Fjord in southern Alaska could generate tsunamis if they failed rapidly and entered the water of the fjord. Landslide A, at the front of the glacier, is the largest, with a total volume estimated at 455 M m3. Historical photographs from Barry Arm indicate that Landslide A initiated in the mid twentieth century, but there was a large pulse of movement between 2010 and 2017 when Barry Glacier thinned and retreated from about 1/2 of the toe of Landslide A. Interferometric synthetic aperture radar (InSAR) investigations of the area between May and November, 2020, revealed a second, smaller landslide (referred to as Landslide B) on the south-facing slope about 2 km up the glacier from Landslide A. Landslide-generated tsunami modeling in 2020 used a worst-case scenario where the entire mass of Landslide A (about 455 M m3) would rapidly enter the water. The use of multiple landslide volume scenarios in future tsunami modeling efforts would be beneficial in evaluating tsunami risk to communities in the Prince William Sound region. Herein, we present a map of landslide structures and kinematic elements within, and adjacent to, Landslides A and B. This map could form at least a partial basis for discriminating multiple volume scenarios (for example, a separate scenario for each kinematic element). We mapped landslide structures and kinematic elements at scale of 1:1000 using high-resolution lidar data acquired by the Alaska Division of Geological and Geophysical Surveys (DGGS) on June 26, 2020 and high resolution bathymetric data acquired by the National Oceanic and Atmospheric Administration (NOAA) in August, 2020. The predominate structures in both landslides are uphill- and downhill-facing normal fault scarps. Uphill-facing scarps dominate in areas where downslope extension from sliding has been relatively low. Downhill-facing scarps dominate in areas where downlslope extension from sliding has been relatively high. Strike-slip and oblique-slip faults form the boundaries of major kinematic elements. Four major kinematic elements, herein named the Kite, the Prow, the Core, and the Tail, are within, or adjacent to Landslide A. One major kinematic element, herein named the Wedge, forms Landslide B. Kinematic element boundaries are a result of cumulative, differential patterns and amounts of movement that began at inception of the landslides. Elements and/or their boundaries may change location as the landslides continue to evolve. Kinematic elements mapped in 2020 may or may not reflect patterns of historical short-term, episodic movement, or patterns of movement in the future. We were not able to field check our mapping in 2020 because of travel restrictions due to the COVID-19 pandemic. We hope to field check the mapping in the summer of 2021. In this data release, we include GIS files for the structural and kinematic map; metadata files for mapped structural features; and portable document files (PDFs) of a location map, and the structural and kinematic map at a scale of 1:5000. Lidar and bathymetric data used to map landslide structures will be released by DGGS and NOAA in 2021.

Two active landslides at and near the retreating front of Barry Glacier at the head of Barry Arm Fjord in southern Alaska could generate tsunamis if they failed rapidly and entered the water of the fjord. Landslide A, at the front of the glacier, is the largest, with a total volume estimated at 455 M m3. Historical photographs from Barry Arm indicate that Landslide A initiated in the mid twentieth century, but there was a large pulse of movement between 2010 and 2017 when Barry Glacier thinned and retreated from about 1/2 of the toe of Landslide A. Interferometric synthetic aperture radar (InSAR) investigations of the area between May and November, 2020, revealed a second, smaller landslide (referred to as Landslide B) on the south-facing slope about 2 km up the glacier from Landslide A. Landslide-generated tsunami modeling in 2020 used a worst-case scenario where the entire mass of Landslide A (about 455 M m3) would rapidly enter the water. The use of multiple landslide volume scenarios in future tsunami modeling efforts would be beneficial in evaluating tsunami risk to communities in the Prince William Sound region. Herein, we present a map of landslide structures and kinematic elements within, and adjacent to, Landslides A and B. This map could form at least a partial basis for discriminating multiple volume scenarios (for example, a separate scenario for each kinematic element). We mapped landslide structures and kinematic elements at scale of 1:1000 using high-resolution lidar data acquired by the Alaska Division of Geological and Geophysical Surveys (DGGS) on June 26, 2020 and high resolution bathymetric data acquired by the National Oceanic and Atmospheric Administration (NOAA) in August, 2020. The predominate structures in both landslides are uphill- and downhill-facing normal fault scarps. Uphill-facing scarps dominate in areas where downslope extension from sliding has been relatively low. Downhill-facing scarps dominate in areas where downlslope extension from sliding has been relatively high. Strike-slip and oblique-slip faults form the boundaries of major kinematic elements. Four major kinematic elements, herein named the Kite, the Prow, the Core, and the Tail, are within, or adjacent to Landslide A. One major kinematic element, herein named the Wedge, forms Landslide B. Kinematic element boundaries are a result of cumulative, differential patterns and amounts of movement that began at inception of the landslides. Elements and/or their boundaries may change location as the landslides continue to evolve. Kinematic elements mapped in 2020 may or may not reflect patterns of historical short-term, episodic movement, or patterns of movement in the future. We were not able to field check our mapping in 2020 because of travel restrictions due to the COVID-19 pandemic. We hope to field check the mapping in the summer of 2021. In this data release, we include GIS files for the structural and kinematic map; metadata files for mapped structural features; and portable document files (PDFs) of a location map, and the structural and kinematic map at a scale of 1:5000. Lidar and bathymetric data used to map landslide structures will be released by DGGS and NOAA in 2021.

This inventory was originally created by Harp and others (1984) describing the landslides triggered by a sequence of earthquakes, with the largest being the M 6.5 Mammoth Lakes, California earthquake that occurred on 25 May 1980 at 19:44:50 UTC. Care should be taken when comparing with other inventories because different authors use different mapping techniques. This inventory includes landslides triggered by a sequence of earthquakes rather than a single mainshock. Please check the author methods summary and the original data source for more information on these details and to confirm the viability of this inventory for your specific use. With the exception of the data from USGS sources, the inventory data and associated metadata were not acquired by the U.S. Geological Survey (USGS) and thus have not been reviewed for accuracy and completeness by the USGS. They are presented as part of this data series for convenience of the user only, as part of an effort to make published ground-failure inventories more accessible from a single aggregated site. No warranty, expressed or implied, is made regarding the display or utility of the data on any other system or for general or scientific purposes, nor shall the act of distribution constitute any such warranty.

This inventory was originally created by Harp and others (1984) describing the landslides triggered by a sequence of earthquakes, with the largest being the M 6.5 Mammoth Lakes, California earthquake that occurred on 25 May 1980 at 19:44:50 UTC. Care should be taken when comparing with other inventories because different authors use different mapping techniques. This inventory includes landslides triggered by a sequence of earthquakes rather than a single mainshock. Please check the author methods summary and the original data source for more information on these details and to confirm the viability of this inventory for your specific use. With the exception of the data from USGS sources, the inventory data and associated metadata were not acquired by the U.S. Geological Survey (USGS) and thus have not been reviewed for accuracy and completeness by the USGS. They are presented as part of this data series for convenience of the user only, as part of an effort to make published ground-failure inventories more accessible from a single aggregated site. No warranty, expressed or implied, is made regarding the display or utility of the data on any other system or for general or scientific purposes, nor shall the act of distribution constitute any such warranty.

This data release contains (1) geotechnical reports describing colluvium strength and grain size distribution, (2) hydrological monitoring data (rainfall and soil volumetric water content), and (3) shapefiles of mapped landslides from 1996 and 2021 that occurred in the Columbia River Gorge, Oregon. The geotechnical reports describe test results from a sieve and hydrometer analysis (ASTM D422) to characterize the grain size distribution and from consolidated drained direct shear tests (ASTM D3080) to characterize soil shear strength. Hydrological data includes a time history of rainfall and volumetric water content from a monitoring station in the Columbia River Gorge, spanning 10/28/2022 to 2/13/2023. The mapped landslide shapefiles represent shallow landslide source areas, assumed to have failed during storms in 1996 and 2021.

We performed a ground-based, interferometric, synthetic aperture radar (InSAR) survey of the Slumgullion landslide located in Hinsdale County, Colorado. The survey was performed 26 June 2010-1 July 2010 and utilized the IBIS-L InSAR system developed by IDS Corporation. Radar measurements were supplemented by hourly in-situ displacement, pore-water pressure, and rainfall measurements. In-situ displacement was measured using electronic cable extension transducers (extensometers) at three locations and GPS surveying at one location. Pore-water pressures were measured at three locations using electronic vibrating-wire pressure transducers (piezometers). Rainfall was measured at one location using a tipping-bucket rain gage. Georeferenced InSAR data were obtained as cumulative line-of-sight displacement of points on and off of the landslide, and in-situ displacement data were obtained as cumulative displacement parallel to the radar line of sight. InSAR data were obtained continuously (hourly) throughout the survey period while in-situ data were obtained sporadically but generally on an hourly basis. These data are associated with a study described in Schulz, W.H., Coe, J.A., Ricci, P.P., Smoczyk, G.M., Shurtleff, B.L., and Panosky, J., 2017, Landslide kinematics and their potential controls from hourly to decadal timescales: Insights from integrating ground-based InSAR measurements with structural maps and long-term monitoring data: Geomorphology, doi:10.1016/j.geomorph.2017.02.011.

We performed a ground-based, interferometric, synthetic aperture radar (InSAR) survey of the Slumgullion landslide located in Hinsdale County, Colorado. The survey was performed 26 June 2010-1 July 2010 and utilized the IBIS-L InSAR system developed by IDS Corporation. Radar measurements were supplemented by hourly in-situ displacement, pore-water pressure, and rainfall measurements. In-situ displacement was measured using electronic cable extension transducers (extensometers) at three locations and GPS surveying at one location. Pore-water pressures were measured at three locations using electronic vibrating-wire pressure transducers (piezometers). Rainfall was measured at one location using a tipping-bucket rain gage. Georeferenced InSAR data were obtained as cumulative line-of-sight displacement of points on and off of the landslide, and in-situ displacement data were obtained as cumulative displacement parallel to the radar line of sight. InSAR data were obtained continuously (hourly) throughout the survey period while in-situ data were obtained sporadically but generally on an hourly basis. These data are associated with a study described in Schulz, W.H., Coe, J.A., Ricci, P.P., Smoczyk, G.M., Shurtleff, B.L., and Panosky, J., 2017, Landslide kinematics and their potential controls from hourly to decadal timescales: Insights from integrating ground-based InSAR measurements with structural maps and long-term monitoring data: Geomorphology, doi:10.1016/j.geomorph.2017.02.011.