# Study on Temporal and Spatial Distribution of Landslides in the Upper Reaches of the Yellow River
## 4 Spatial Distribution Characteristics of Giant Landslides in the Upper Reaches of the Yellow River
\) & \(101^{\circ}53^{\prime}46^{\prime\prime}\) & \(36^{\circ}06^{\prime}04^{\prime\prime}\) & 300 & 0.35 & 30 \\ \cline{2-8}  & & HP13 & \( \begin{array}{c}\text{Mud flat}\\ \text{landslide}\end{array} \) & \(101^{\circ}58^{\prime}58^{\prime\prime}\) & \(35^{\circ}59^{\prime}55^{\prime\prime}\) & 372 & 0.86 & 20 \\ \cline{2-8}  & & HP14 & Locked slide & \(102^{\circ}03^{\prime}41^{\prime\prime}\) & \(35^{\circ}54^{\prime}40^{\prime\prime}\) & 250 & 13.55 & 48 \\ \hline  & & HP15 & \( \begin{array}{c}\text{Root}\\ \text{landslide}\end{array} \) & \(102^{\circ}32^{\prime}53^{\prime\prime}\) & \(35^{\circ}46^{\prime}43^{\prime\prime}\) & 400 & 1.08 & 25 \\ \cline{2-8} Recirculating basin & & HP16 & \( \begin{array}{c}\text{Chaligang}\\ \text{landslide}\end{array} \) & \(102^{\circ}21^{\prime}12^{\prime\prime}\) & \(35^{\circ}53^{\prime}57^{\prime\prime}\) & 500 & 0.39 & 25 \\ \cline{2-8}  & & HP17 & \( \begin{array}{c}\text{Tangiacatan}\\ \text{landslide}\end{array} \) & \(102^{\circ}14^{\prime}20^{\prime\prime}\) & \(35^{\circ}14^{\prime}20^{\prime\prime}\) & 305 & 2.40 & 30 \\ \cline{2-8}  & & HP18 & \(\begin{array}[]  
Field investigation and remote sensing image analysis show that the width of the front and back edges of the giant landslide in the study area and the length and width of the slide body are similar. The relative elevation difference between the top of the back edge of landslide deposits and the shear outlet of the leading edge has three peaks, which are located at 350 m, 550 m, and 750 m, respectively, and the maximum can reach 875 m. This is basically consistent with the results of the relative height difference between high and steep slopes in the basins on both sides of the main stream of the Yellow River. The back wall of most landslides is well preserved, and the slope of the landslide is mostly between 25\({}^{\circ}\) and 40\({}^{\circ}\). For example, the average slope of the Xiaangtan landslide located in the Qunke-Jianzha Basin is 26.4\({}^{\circ}\). During the sliding process of the landslide, the front topography reversed, and the water in the middle of the landslide formed a landslide lake with a depth of 26.4 m.  
The distribution of landslides in the Sigovxia and Laganxia sections of the upper reaches of the Yellow River is affected and restricted by environmental factors such as landform, stratigraphic lithology, active structure, and climate change. Through remote sensing images and field investigation, it was found that the landslides in the study area are mainly distributed in Qunke-Jianzha Basin, accounting for 29.3% of the total investigated, followed by Xinhua Basin, Gonghe Basin, Guanting Basin, Guide Basin, Laxiwa Gorge, Lijia Gorge, Jishi Gorge, and Gongbo Gorge. The south bank of the Yellow River has more landslides than the north bank. For example, the Guide Basin and Qunke-Jianzha Basin on the south bank have extremely large-scale and high-intensity development, while the north bank has relatively few landslides. The spatial distribution characteristics of landslides are closely related to the factors of landform, active structure, and climate change in the study area. In the process of landslide formation and development, one or several factors may play the main controlling role. From the analysis of the age of landslide development, ancient landslides and old landslides are the most developed landslides in the study area, and the slide distance is relatively long, belonging to the high-speed remote landslide type. Some landslide slopes once blocked the Yellow River, leaving a large number of landslide remnants on the other side of the Yellow River. For example, the Golongbu landslide (semi-consolidated rock landslide) in the Jishi Gorge area, the Suozi landslide (bedrock landslide), and the Xiaangtan landslide (mudstone landslide) in the Qunke-Jianzha basin.