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Exploring the groundwater response to rainfall in a translational landslide using the master recession curve method and cross-correlation function
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Abstract: Rainfall is a common trigger for landslide reactivation, as it raises groundwater levels and reduces bedrock or soil shear resistance. This study focuses on the Kualiangzi landslide in the southern region of Sichuan Province, China. Real-time monitoring of groundwater levels and rainfall from July 2013 to September 2016 is analyzed. Groundwater table increments, considering groundwater drainage rate, were calculated using the water-table fluctuation and master recession curve method and the response time of the groundwater table to rainfall events was estimated using the cross-correlation function. Results reveal that groundwater level declines from tension troughs to landslide fronts in the rainy season, with a significant positive correlation between the groundwater level in the tension trough and landslide surface displacement. Evaluated spring elevations for groundwater discharge range from 410 m to 440 m, which is in agreement with the actual spring elevations (390–423 m). Lag times of groundwater response to rainfall decreases with cumulative rainfall of the rainy periods. In the middle part of the landslide, two responses between rainfall and groundwater levels indicate two water movement pathways: Vertical cracks or fractures resulting from the slow landslide movement, and matrix pore space in unconsolidated sediment. Variations in peak values of the cross-correlation function suggest early dominance of the uniform matrix flow and later dominance of preferential flow during the rainy period.
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Key words:
- Translational landslide /
- Rainfall /
- Groundwater /
- Lag response /
- Water table fluctuation /
- Recharge pathway
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Figure 1. Study area
(a) Location of the study area in Sichuan Province. (b) Tectonic outline map in the Zhongjiang District. (c) Geological schematic map of the Kualiangzi landslide. (d) Geological profile of section I-I' (modified from Ling et al. 2016). The geographic data set is provided by Geospatial Data Cloud site, Computer Network Information Center, Chinese Academy of Sciences
http://www.gscloud.cn ).
Figure 2. Lithology, stratum thickness, and water level sensors in the boreholes U1-1, U1-3, U1-4, U1-5, and P1-3. The maximum and minimum of the water table in each borehole were obtained from 1 June 2013 to 12 September 2016.
Note: the length and surface elevation of each borehole were drawn on a same vertical scale, but not a same horizontal scale.
Figure 3. Schematic diagram for calculating the groundwater table increment by a rainfall event
(a) The measured water level process line after a rainfall event. (b) The relationship between measured water level (H) and drainage rate (D>0) if the groundwater level varies with a large range. (c) The corrected groundwater table increment considering the drainage rate of the groundwater.
Figure 5. Daily variations in rainfall, surface displacement, and groundwater level from 1 June 2013 to 12 September 2016. The rainfall recorder and its cable were destroyed by the creeping of landslide on 8 December 2015, which makes the rainfall data from 8 December 2015 to 1 June 2016 missing. The increment in groundwater level (i.e. U1-1) in the tension trough almost kept pace with the displacement rate of the landslide
Figure 6. Relationship between groundwater level in borehole U1-1 and displacement rate of GPS01.
Figure 7. Relationship between measured water level (H) and drainage rate (D) in boreholes (a) U1-1, (b) U1-3, (c) U1-4, (d) U1-5, and (e) P1-3. The fitted equations relating H and D and their coefficient of determination (R2) are also given. $ {\mathit{H}}_{0} $ is the evaluated elevation of springs for the groundwater discharge
Figure 8. Daily variations in (a) rainfall and groundwater level increment in boreholes (b) U1-1, (c) U1-3, (d) U1-4, (e) U1-5, and (f) P1-3.
Figure 9. Monthly variations in cumulative rainfall and water level increment in borehole U1-1, and Box-Whisker plots of hourly rainfall in (a) 2013, (b) 2014, and (c) 2015. The values of median (50) and quartiles (75) were also given in the figures.
Figure 10. Hourly variations in rainfall and groundwater level increment from 20 June 2013 to 7 August 2013. The time series of rainfall are divided into three events. The first event was the period from 20 June 0:00 to 29 June 17:00. The second event was the period from 29 June 18:00 to 15 July 18:00. The third event was the period from 15 July 19:00 to 7 August 23:00.
Figure 11. Cross-correlation between rainfall and groundwater level increment for boreholes (a) U1-1, (b) U1-3, (c) U1-4, (d) U1-5, and (e) P1-3.
Figure 12. Electrical resistivity tomography results: (a) the profile A-A' on 19 September 2014; (b) resistivity ratios of the A-A' profile on 19 September 2014, considering the data set of 28 February 2014 as a reference (Modified from Ling et al. 2016).
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