Mapping methodologies used to map landslides along King County river corridors
Tools for evaluating and identifying landslide hazards are continuously evolving. A review of technical literature and consultation with subject matter experts were used to identify and use the most current and appropriate methodologies for the various types of landslide hazards identified in the study. The mapping methods selected were appropriate for mapping at a landscape scale. More accurate assessments of the potential for landsliding at a specific location are possible based on site-specific investigations and assessment methods that account for site-specific conditions.
The advent of LiDAR and the data and imagery derived from it have revolutionized landslide mapping over the last decade. The topographic data generated from LiDAR shows the ground surface topography at a resolution unattainable with any other imaging technology. Remote detection of subtle yet important topographic features, even where covered by mature forest, is possible by visual inspection of LiDAR-derived hillshade images, as seen in the figures below. In addition to LiDAR imagery, geologic maps prepared by the U.S. Geological Survey and by the Washington Department of Natural Resources were utilized (see Map References in Section 8.0 – References of report).
Tolt Valley RM 3.5 to 4.6 topographic detail for comparison using (a) LiDAR, (b) aerial photography, and (c) USGS topographic mapping
This project identified five types of landslide hazards in King County:
- Deep-seated landslides
- Shallow debris slides
- Depositional fans, consisting of the following
- Rock fall
- Rock avalanches
King County retained Shannon & Wilson, Inc. to map deep-seated landslides within the study limits using the procedure in the Oregon State Department of Geology and Mineral Industries (OR DOGAMI) Special Paper 42 (Burns and Madin 2009). Shannon & Wilson, Inc. mapped 930 deep-seated landslides in the study area during this work. A report prepared by Shannon & Wilson, Inc. to accompany their mapping is included as Appendix A of the report.
Many features of deep-seated landslides share similar topographic characteristics including steep, often arcuate head scarps defining the upslope limit of the slide and a distinct deposit of displaced debris downslope. The debris was often identifiable by its lobate form and hummocky upper surface. These features varied in their topographic distinctness from features that appeared sharp and unambiguous to features that were muted and subtle. It is likely that some features mapped as slides based on their topographic character may have formed in other ways and it is also likely that some prehistoric deep-seated landslides present in the study limits were not identified because they were not distinguishable with the available imaging.
The landslide features identified by Shannon & Wilson, Inc. following the DOGAMI method are noted in the figure below.
A numerical confidence rating method set by the DOGAMI method (e.g., headscarp and slide morphology) was used to assign ratings to each mapped landslide. Twenty attributes, i.e. relative age of landslide, LiDAR source and date, and whether the slide appeared natural or human modified, of each landslide, were documented.
Shallow debris slides
The stability of slopes with respect to shallow debris failures is often evaluated using a simple limit equilibrium analysis known as the infinite slope model. The infinite slope model is the only commonly used quantitative slope stability model applicable across an entire landscape. For this DNRP mapping project, an infinite slope analysis was used to generally identify slopes potentially subject to shallow debris slides. Soil strength parameters were estimated by measuring the inclination of 45 valley-wall slopes in the study limits that were relatively straight in profile. Following the DOGAMI protocol (Burns et al. 2012), slopes of 24 degrees to 28 degrees (44 to 54 percent) were identified as having a FOS between 1.25 and 1.5 and having a moderate hazard of being subject to shallow debris slides. Slopes steeper than 28 degrees (54 percent) were identified as having a FOS of less than 1.25 and having a severe hazard of being subject to shallow debris slides. The figure below shows how the moderate and severe hazard for potential shallow debris slides is mapped in an area of (a) the Cedar River basin and (b) the Snoqualmie River basin.
This section addresses methodologies used to map fans and differentiate within the fans located in alpine areas within the study limits those that are either more or less likely subject to debris flows. The figure below summarizes the methodology followed and shows the decision making criteria for identifying all fans (Section 4.4.1 of report), addressing large alluvial fans (Section 4.4.2 of report), mapping all fans in Puget Lowland areas (Section 4.4.3 of report) and mapping alpine fans that are either more or less likely to be subject to debris flows (Section 4.4.4 of report).
A depositional fan is physical evidence of the extent of past debris deposition, and these features often are indicators of future inundation. These depositional fans tend to be relatively low-gradient and are not readily apparent from hillshade imagery (see left figure below). However, when looking at closely spaced (5-foot) contour interval lines derived from high resolution, LiDAR-derived topography, the conical shape of a fan is more clearly evident. The figure below on the right shows an example of the closely spaced contours and LiDAR imagery used for this mapping method.
Maplewood Creek fan on the Cedar River near RM 3.5. Fan is shown using (a) LiDAR hillshade imagery and (b) more clearly identified when utilizing 5-foot contour interval lines.
Another distinguishing characteristic of both alluvial and debris fans is that they form where sediment deposition occurs where there is an abrupt change in gradient from a steep source area upslope to a lower gradient receiving area below. Most fans are associated with a topographically distinct drainage channel that joins the fan at its apex. Fans created by rock fall or raveling may not have a contributing channel. It is common for the channel to be significantly incised into the fan where it crosses the fan surface. This sort of incision may indicate that the fan is a relict feature from some prior climatic/landscape regime (immediate post-glacial time, for example). In this report, all fans including those with incised channels are mapped unless the magnitude of the incision precludes all plausible channel relocation.
Puget Lowland fans
No simple metric was identified in the literature that could be used to screen lowland basins and identify those most likely to be inundated by such debris flows. A review of sites with known recent debris flows or debris floods in the Puget Lowland areas of King County suggests that they share some characteristics in common:
- All of the recent incidents reviewed entailed discharge from ravines with steep side slopes, typically > 60 percent slopes;
- All discharged onto well-defined, preexisting fans, and these flows were often initiated by a sudden release of water, and in a number of recent cases this has been the result of failure of an upstream beaver dam;
- Where the channel gradient above the fan was steep, in excess of a 15 percent slope, the discharge was in the form of a debris flow; and
- Where the channel gradient was less than a 15 percent slope, the discharge took the form of a debris flood.
These observations are based on a small number of recent incidents, which is not enough to develop robust screening criteria. Based on the characteristics above, DNRP geologists used LiDAR imagery and closely spaced contour lines to map depositional fans in the Puget Lowland areas.
Alpine fans either more or less subject to debris flows
Research in British Columbia has identified a simple landscape metric that identifies alpine drainage basins that are more likely to produce debris flows (Wilford et al. 2009). This metric is variously known as the Relative Relief Ratio (used here) or the Melton Ratio (see figure below). The ratio increases with the elevation range of the basin and decreases with the square root of the basin area. The ratio will therefore be greatest for small basins that span a large elevation change. Research in British Columbia has shown that basins with a Relative Relief Ratio of 0.6 or more are more likely to produce debris flows, and that fans with a Relative Relief Ratio less than 0.6 are more likely to produce debris floods or normal fluvial flooding (Wilford et al. 2009).
The CONEFALL software program was used to implement this approach in a GIS environment to map areas where rock fall could propagate downslope from a source. As a starting point for the CONEFALL program, cliff-faces were identified to delineate the line representing the base-of-cliff/top-of-talus. Within the study limits, these lines were mapped based on professional judgment using a variety of tools in a GIS environment including vertical orthophotography, oblique photography, and slope mapping. Slopes inclined at more than 200 percent were especially identified.
An example of the output from CONEFALL for the Mt. Si area is shown in the figure below, where boulders are mostly mapped within the CONEFALL modeled area around the base of Mt. Si. It is important to note that the integrity of the bedrock was not considered in this model.
This figure shows an example of the output from CONEFALL for the Mt. Si area where boulders are mostly mapped within the CONEFALL modeled area at around the base of Mt. Si. It is important to note that the integrity of the bedrock was not considered in this model.
Rock avalanche deposits
Rock avalanche deposits were identified within the study limits using USGS geologic maps, review of LiDAR imagery, interpretation of orthophotography, field investigation, and geotechnical reports. The figure below is an example of a rock avalanche deposit mapped in the South Fork Skykomish River valley. Due to the lack of detailed information on significant variables including rock strength, zones of weakness and joint patterns, predictions of future sites of rock avalanches were not feasible.
This figure shows the Beckler Peak Rock Avalanche deposit mapped in the Skykomish River valley: the orange tint shows the extent of the deposits which originated on the south face of Beckler Peak and filled the lower Tye and upper South Fork Skykomish River valleys.