Liquefaction potential for the Kathmandu Valley, Nepal: a sensitivity study

An assessment of liquefaction potential for the Kathmandu Valley considering seasonal variability of the groundwater table has been conducted. To gain deeper understanding seven historical liquefaction records located adjacent to borehole datapoints (published in SAFER/GEO-591) were used to compare two methods for the estimation of liquefaction potential. Standard Penetration Test (SPT) blowcount data from 75 boreholes inform the new liquefaction potential maps. Various scenarios were modelled, i.e., seasonal variation of the groundwater table and peak ground acceleration. Ordinary kriging, implemented in ArcGIS, was used to prepare maps at urban scale. Liquefaction potential calculations using the methodology from (Sonmez, Environ Geol 44:862–871, 2003) provided a good match to the historical liquefaction records in the region. Seasonal variation of the groundwater table is shown to have a significant effect on the spatial distribution of calculated liquefaction potential across the valley. The less than anticipated liquefaction manifestations due to the Gorkha earthquake are possibly due to the seasonal water table level.


Introduction
The Kathmandu Valley is located approximately 10 km from the Main Himalayan Thrust (MHT) (Elliott et al. 2016). This geographical area experienced several destructive earthquakes in the past: the latest significant event occurred in 2015, the M w 7.8 Gorkha earthquake (Grandin et al. 2015). The Gorkha earthquake caused structural damage and geotechnical failures, including landslides and liquefaction (e.g., Goda et al. 2015;Chiaro et al. 2015;Hashash et al. 2015;Moss et al. 2015;Sharma and Deng 2019). The thick, sediments underlying the Kathmandu Valley have highly variable geotechnical properties (e.g., Sakai et al. 2008;Gilder et al. 2020) and are prone to liquefy (e.g., Rajendran et al. 1 3 2016). However, the study of Moss et al. (2017) demonstrated that evidence of liquefaction in the aftermath of the 2015 Gorkha earthquake was less significant than expected. Possible reasons for this may include: changes in the groundwater table due to extraction (e.g., Pandey et al. 2012); seasonal variation of groundwater table level (Shrestha and Tamrakar 2018) and/or underestimation of soil stiffness (e.g., V S30 ) (cf. Wald and Allen 2007). Jha et al. (2020) compared probabilistic and deterministic approaches for liquefaction potential evaluation in the Kathmandu Valley using two boreholes. In this paper, two deterministic approaches (Iwasaki et al. 1978, 1982and Sonmez 2003) are compared using a database of field observations. The observations of Moss et al. (2017) are also tested in this paper.
For the Kathmandu Valley, geotechnical testing Pokhrel et al. 2019a) and the collection of historical geotechnical investigations (Gilder et al. 2020) have shown that the slope-based prediction of shear wave velocity represents an overestimation for many areas of the valley (Gilder et al. 2018;De Risi et al. 2021). In data-scarce regions, such as the Kathmandu Valley, geostatistical tools may be used to extrapolate results from point locations to a geographical area (e.g., De Risi et al. 2021). Kriging interpolation is often used to determine values for liquefaction potential measures at locations without sufficient geotechnical data (e.g., Baise and Lenz 2006;Maruyama et al. 2010;Pokhrel et al. 2010Pokhrel et al. , 2013Pokhrel et al. , 2012Thompson et al. 2010;Chung and Rogers 2011;Baker and Faber 2008;Liu andChen 2006, 2010;Habibullah et al. 2012).
Three new records of liquefaction and four previously documented records of liquefaction within the Kathmandu Valley are examined in this paper. These records are all located in the vicinity of borehole locations collected in the geo-database SAFER/GEO-591 (Gilder et al. 2019b(Gilder et al. , 2020. In this paper, the two reviewed approaches for liquefaction potential determination use the triggering model from Seed and Idriss (1971) and the manifestation models by Iwasaki et al. (1978Iwasaki et al. ( , 1982Iwasaki et al. ( , 1984 and Sonmez (2003) respectively. These approaches are compared against the liquefaction records examined in this study to enable comment on which is the most applicable 'simplified' method for the valley. The approaches are implemented using data from 75 borehole locations (see Table 1) along with the kriging algorithm from ArcGIS to prepare liquefaction maps for variable PGA values and groundwater table levels. Another possible use of SAFER/GE0-591 is to use the data to estimate building settlements (based on SPT N 60 ) using methodologies such as that described in Valverde-Palacios et al. (2014).

Geology
The Kathmandu Valley is an intermontane basin in the Lesser Himalayas in central Nepal, south of the Great Himalayan Range (e.g., Sakai et al. 2008). The valley is made up of: (a) a basement, metamorphic rock underlying the valley at depth, and (b) younger valley sediments which overly the metamorphic rock formations. Figure 1 shows the liquefaction map of the UNDP/UNCHS (HABITAT) (1993) Subproject "Seismic hazard mapping and risk assessment for Nepal". This project was important as new surficial geological maps were developed based on the details of well data sources originating from the early work done in the Valley. Similarly, the geomorphological map of Yoshida and Igarashi (1984) (Fig. 1b) described a number of sediments resulting from both the Quaternary deposition (recent 1 3 sediment deposits near rivers) and earlier Pliocene to Pleistocene deposits from a variety of depositional environments including fluvio-deltaic, laucustrine and deltaic (Sakai et al. 2008). The geological map in Fig. 2 indicates the newer geological designations from Shrestha et al. (1998). The Kalimati Formation beneath any recent deposits in the central Valley ( Fig. 1c) (Paudel and Sakai 2009) often consists of a laminated black clayey, silt interlaminated with silt, clay and with very fine, silty, sand layers. The Sunakothi Formation, present in much of the southern part of the Valley, contains both clayey sequences and laminated silts and sands. The Terrace deposits contain coarser materials, skirting the bedrock geology of the southern central and western margins. When examining Fig. 1b, it can be seen how the original liquefaction map (Fig. 1a) was defined. Where rivers are present (with presumably saturated soils) these areas represent the position of highest liquefation potential. This potential reduces towards the valley edge. More recent assessments have indicated that the highest potential is at locations near the rivers and in the central valley (Gautam et al. 2017), and probabilistic assessments have reported similar findings (Sajan et al. 2020;Khatakho et al. 2021). However, this has been attributed to the older sequences and as the Valley contains a complex mix of laminated sequences it remains a challenge to evaluate the liquefaction potential in the valley. It is likely much of the valley mapping is affected by recent superficial deposits (which are not currently shown on maps) due to the likely occurance of channel movement and geomorphic development of the river basin (Shrestha and Tamrakar 2013). Age relationships of the soils shown in Fig. 1 are inexact due to the combination of map sources. For instance, more recent Cone Penetration Testing (CPT) work has suggested that some locations near rivers are unlikely to liquefy ) but also the position of the Araniko Highway movement is upon a relict river channel. These conclusions ) are also currently affected by the ability to assess the silts of this region for liquefaction potential due to the limited amount of geotechnical field and laboratory testing. Herein, the aim is to improve understanding of potential seasonal variation of liquefaction potential and to compare the modelled results to observations taken following the 2015 Gorkha earthquake. Table 2 lists the significant historical earthquakes recorded in the Kathmandu Valley. The most devastating earthquakes occurred in 1833, 1866, 1934(Rana 1935Bilham 1995Bilham , 2019Pandey et al. 2002;Pandey and Molnar 1988;Goda et al. 2015). Prior studies considered a fault system containing three main faults, namely the main central thrust (MCT), main boundary thrust (MBT) and himalayan frontal thrust (HFT) (e.g.,  Yoshida and Igarashi (1984), digitised map data from Yoshida and Gautam (1988) c map of Plio-Pleistocene sediments, digitised map data from Paudel and Sakai (2009) 1 3 Chaulagain et al. 2015). The maximum PGA generated for the Kathmandu Valley by the earthquakes from these thrusts is around 0.35 g; consistent with the old building code of Nepal (1994) (NBC 1994). Publications after the 2015 Gorkha earthquake have better described the geometry of the main himalayan thrust (MHT) beneath the Kathmandu  Table 6 and zoomed areas to indicate distance between the liquefaction point identified in this study (black triangle) and validation borehole (red circle). The historical liquefaction points evidenced by the field study Geotechnical Extreme Event Reconnaissance (GEER) (locations given in Hashash et al. 2015) are also shown (red triangles). Recent deposits have been added to map data digitised from Shrestha et al. (1998) map to reflect true extent of rivers Valley (Elliott et al. 2016) and highlighted that the MHT could generate an earthquake as great as magnitude M W 9.0 (Stevens et al. 2018;Pokhrel et al. 2019b). The new building code for Nepal (NBC 2020), specifies a maximum PGA value for the Kathmandu valley of 0.35 g for a 475-year return period. PSHA results are significantly affected by the specific choice of GMPEs assumed (Stevens et al. 2018;De Risi et al. 2020). Taking the MHT as a single seismogenic source, the PGA can vary significantly depending on the GMPE used.

Groundwater level and water table
Nepal lies in a humid-subtropical climatic region with dry-winters (Kottek et al. 2006) and heavy rain-summers. During the rainy seasons, monsoons last from mid-June to mid-September (approximately 90 days) during which time the average rainfall is more than 1000 mm (Pokharel and Hallett 2015). However, the seasonal variation of the groundwater table for particular deposits was not explicitly considered. Shrestha and Tamrakar (2018) mapped the shallow groundwater level for dry (pre-monsoon) and wet (monsoon) season in the northern part of the Kathmandu Valley. In particular, data from 239 wells were collected during wet and dry season, allowing an average estimation of seasonal variation of the groundwater level. In this study, using the observations of Shrestha and Tamrakar (2018): • 1.6 m is taken as the approximate value for the water table in the wet season, estimating it as the average depth minus one half of the standard deviation from the data reported in Shrestha and Tamrakar (2018). • 5.1 m is taken as the approximate value for the water table in the dry season, estimating it as the average depth plus one half of the standard deviation from the data reported in Shrestha and Tamrakar (2018).
These assumptions do not allow for the spatial variation of the groundwater table (cf. Fan et al. 2013). However, the aim herein is to study seasonal variation of the groundwater table in conjunction with variability of the PGA as obtained from recent probabilistic hazard assessment studies. Seed and Idriss (1971) proposed a method to assess liquefaction resistance of soils. In this approach, the factor of safety against liquefaction (F L ) is determined by the ratio between the cyclic resistance ratio (CRR) and the earthquake-induced cyclic stress ratio (CSR) (see Sonmez (2003) for further commentary on the historical development of this approach). This method is widely used as a triggering model to evaluate the factor of safety against liquefaction F L (e.g., Geyin et al. 2020). F L is used to evaluate if a soil layer is susceptible or non-susceptible to liquefaction during an earthquake. Iwasaki et al. (1984) proposed a liquefaction potential index (I L ) to evaluate the liquefaction potential in multiple layers of soil. The liquefaction potential index (I L ) in Iwasaki et al. (1984) is referred to in this paper as the liquefaction potential (P L ); this parameter assumes that surface manifestation depends on the thicknesses of all strata that can liquefy in the uppermost 20 m of a soil column, their proximity to the ground surface, and the amount by which the factor of safety against liquefaction in each stratum (F L ) is less than 1.0 (Geyin et al. 2020). The methodology of Iwasaki et al. (1984) was also used in the work of Piya et al. (2004) who presented both qualitative and quantitative liquefaction potential assessments for the Kathmandu valley using the available SPT data at that time.

Liquefaction potential calculation
Equation 1 gives the function of the liquefaction resistance factor, F(z), is expressed through Eq. 2 and the depth weighting factor, W(z), is expressed through Eq. 3 in which z represents the depth of the midpoint of the soil layer from the surface. Sonmez (2003) modified P L based on data from Inegol (Turkey) and Sonmez and Gokceoglu (2005) modified P L based on data from Yuanlin (Taiwan). The assumption for F(z) to be used in Eq. 1 was modified according to Eq. 4 to incorporate marginally liquefiable strata ('moderate') (characterised by F L in the range [0.95-1.2], Sonmez (2003)).
Comparison of the approaches of Iwasaki et al. (1984) and Sonmez (2003) was also presented in Liu (2008). In the present study, the methodologies by Iwasaki et al. (1984) and Sonmez (2003) were used to evaluate the liquefaction potential in the Kathmandu valley using new case evidence from the Gorkha earthquake and geotechnical investigations from the SAFER/GEO-591 geo-database (Gilder et al. 2019b). Table 3 shows the D 50 and ρ soil values used for the liquefaction potential analysis. Figure 3 shows the grain-size distribution curves from the SAFER/GEO-591 geo-database against the "liquefiable" and "potentially liquefiable" bounds from Tsuchida (1970) and Koester and Tsuchida (1988). These distribution curves are mainly concentrated in the liquefiable boundary emphasising a potential for high susceptibility.

Historical records of liquefaction in the Kathmandu Valley
Photographs taken immediately after the Nepal-Bihar earthquake show fractures developed in the field associated with sand boiling (Rana 1935). After the Nepal-Bihar earthquake, eyewitness accounts describe liquefaction evidenced by observations of sand boiling and soil fissuring. Photographic reports from Rana (1935) show "ground fissures after sand boiling" in the central part of Kathmandu city (location 5 in Fig. 2), in Tundikhel (Rana 1935). Similarly, during the 2015 Gorkha earthquake further evidence was observed.   Fig. 3 Grain-size distribution curves from SAFER/GEO-591, liquefaction bounds attributed to Tsuchida (1970) digitized from Koester and Tsuchida (1988) located near to boreholes locations in the SAFER/GEO-591 geo-database also reported in Fig. 2. In Fig. 2 the locations evidenced in the geotechnical extreme event reconnaissance (GEER)  and Table 4) field studies are compared. Those that do not feature in Table 6, did not have an accompanying quality borehole record. In Table 5 the locations from this study are detailed, locations 7a, 7b and 7c represent new data collected in the aftermath of the Gorkha earthquake by the first author. All evidence data (i.e., photographic documentation and borehole details from SAFER/GEO-591) are provided in this paper (Tables 1, 4 and 5 and Figs. 10,11,12,13,14 and 15 in the Appendix). The P L and the corresponding liquefaction potential category according to Iwasaki et al. (1984) and Sonmez (2003) are compared: both methodologies give similar computed values of liquefaction potential with Sonmez providing slightly higher P L values (see Table 6) leading to a refined estimate. However, both estimates remain quite similar. Figure 4 shows a ground fissure at Kausaltar, Bhaktapur (Location 7a in Fig. 2), after the 2015 Gorkha earthquake. Figure 5a shows evidence of a building tilted due to liquefaction effects; this building was situated near the Araniko Highway, corresponding to Location 7b in Fig. 2. Figure 5b shows the liquefaction evidence record for Location 7c in Fig. 2.    Photo/ Rana (1935) and Borehole data from Katel et al. (1996)  No liquefaction observed (Fig. 13) 1 For the Gorkha earthquake PGA was estimated from the USGS Shakemap of the April 25, 2015 event, for 1934 Bihar-Nepal PGA was estimated from a macro-seismic map (Sapkota et al 2016) and regression curve (Wald et al. 1999) 2 The photo evidence was collected by the first author in the aftermath of the Gorkha earthquake, see the Appendix; the same liquefaction location was also documented in another study (Jha et al. 2020) 3 This is an historical record with location name (Tundikhel) on photograph, there is only one Tundikhel in Kathmandu. The photo reflects the location of the liquefaction evidence, but the exact distance cannot be determined 4 Two photos available for evidence at the same site Photographic evidence collected by the first author in the aftermath of Gorkha earthquake and located in the vicinity of three boreholes from the SAFER/GEO-591 database (Gilder et al. 2019b) showed no evidence of liquefaction. These locations are indicated as 8, 9 and 10 in Table 6 are employed as "evidence of no liquefaction" to compare the performances of the two approaches of Iwasaki et al. (1984) and Sonmez (2003). For all three IDs 8, 9 and 10, the resulting P L value is 0 predicting very low and non-liquefiable potential categories for Iwasaki et al. (1984) and Sonmez (2003), respectively (see Table 6). Sonmez's (2003) methodology was found to be better suited for classification of computed P L values based on the evidence presented in this paper for the Kathmandu Valley. Application of the methodology can provide P L estimates at 75 discrete locations using SAFER/ GEO-591 (Gilder et al. 2019b) (see Table 1 for a list of the boreholes used from SAFER/ GEO-591). The final number of boreholes employed is due to the selection of higher quality investigations i.e., the deepest boreholes are used with availability of other geotechnical information) when multiple investigations are available at the same site. To draw liquefaction potential maps for the region kriging interpolation can be used. Kriging interpolation allows for the degree of variation among known data points and corresponding distance to estimate values in unknown areas (e.g., Baise et al. 2006;Thompson et al. 2010;Chung and Rogers 2011;Pokhrel et al. 2012Pokhrel et al. , 2013Thompson et al. 2014). In this paper, the adopted algorithm is the ordinary kriging approach implemented in ArcGIS (ESRI 2012). Given kriging is an interpolation method and that soils are highly variable the results from the maps shown in this paper should not be used for site-specific design work but rather as a useful guide for planning future infrastructure developments.

Seismic hazard
PGA values for the Kathmandu Valley are those based on the PSHA results provided by Stevens et al. (2018). As discussed in several studies (e.g., Stevens et al. 2018;Pokhrel Fig. 4 Liquefaction and cracks in the ground at Kausaltar, Bhaktapur, Nepal, after the 2015 Gorkha earthquake, (Location 7a on Fig. 2). Photograph taken on 2015-05-31 [ De Risi et al. 2020), the hazard in the region is dominated by the MHT; however, the study by Stevens et al. (2018) considered several additional sources contributing to the hazard. Furthermore, the assumption related to the GMPEs in the PSHA can significantly affect hazard results. There remains significant uncertainty related to the choice of GMPEs for PSHA studies in the Himalayan region and the lack of regional GMPEs supported by a significant number of data (e.g., Bajaj and Anbazhagan 2019). Stevens et al. (2018) employed an equally weighted logic tree in their PSHA, i.e., using an average of four GMPEs. Additionally, each GMPE was considered separately (data available in Stevens 2020).
The PGA maps for a probability of exceedance of 2% and 10% in 50 years are considered as they refer to the near-collapse and life safety reference in many international seismic codes (e.g., CEN 2004). The estimates of PGA employed for the Kathmandu Valley in this study are: (i) the final values provided in Stevens et al. based on the average of the four GMPEs considered defined as AVERAGE in the following and (ii) the PGA estimate resulting from the use of the GMPE from Atkinson and Boore (2003) indicated in the following as AB03. The first assumption was the inclusion of GMPEs suitable for crustal and subduction zones, and none of them being region-specific for the Himalaya given the lack of data and the further necessity to develop reliable GMPEs for the area (see also Bajaj and Anbazhagan 2019). The second assumption refers to the subduction GMPE proposed by Atkinson and Boore (2003), which is not region-specific but can be used as a lower bound for PGA for the Kathmandu Valley. Figures 6 and 7 show the PGA maps for the 2% and 10% in 50 years probability of exceedance considering both the AVERAGE (Fig. 6) and AB03 (Fig. 7) GMPE assumptions. Both PGA maps were calculated accounting for the local soil amplification in the basin. This was achieved using the V S30 used as the parameter for soil characterization using the GMPEs. The source for V S30 used in the GMPEs for the PSHA study (Stevens et al. 2018) was the USGS slope-based study by Wald and Allen (2007) and Allen and Wald (2009). This approach tends to overestimate the V S30 values (i.e. soil-stiffness) with respect to direct measurements, as shown in Gilder et al. (2018). For the geomorphological condition and complex geology of the Kathmandu Valley, the slope model does not represent an accurate approximation of V S30 (De Risi et al. 2021) but it is considered suitable at this stage for the scope of zoning liquefaction potential.

Results and discussion
The results are presented for a range of PGA values, obtained from an average representing several GMPEs, (GMPE AVERAGE of Stevens 2020) and a single GMPE (AB03 of Stevens 2020) as shown in Fig. 6 and Fig. 7. These figures indicate the uncertainty in the prediction. The geographical resolution of the data is at the order of approximately 1000 m.
At each borehole location in the SAFER/GEO-591 database used for the liquefaction potential analysis, two different seasonal values of water table depth were used (1.6 m and 5.1 m) as discussed in Sect. 2. Figure 8a and b show the liquefaction potential map of the Kathmandu Valley based on PGA considering the AVERAGE GMPE assumption for 2% in 50 years probability of exceedance under a wet scenario and dry scenario, respectively. Similarly, Fig. 8c and d present 10% in 50 years probability of exceedance in a wet scenario and dry scenario, respectively. Among these, the PGA having 2% probability of exceedance in 50 years is around 1.2 g, and it is almost uniform across the valley. This represents the worst-case scenario of a wet season earthquake where both the sandy deposits and silty or fine-grained materials (characterizing the southern valley) are saturated and so have the potential to liquefy. On the other hand, the PGA for a probability of exceedance of 10% in 50 years is around 0.65 g, and it is more spatially variable (i.e., borehole to borehole). Severe liquefaction is anticipated all around the Kathmandu valley for these PGA values and with an assumed depth of groundwater table of 5.1 m during the dry season. In this scenario, most of the Kathmandu Valley has a high computed potential for liquefaction. Similarly, Fig. 9a and b present liquefaction potential maps of the Kathmandu Valley based on PGA considering only the AB03 GMPE for 2% in 50 years probability of exceedance under a wet scenario and dry scenario, respectively. Figure 9c and d show the liquefaction potential for 10% probability of exceedance in 50 years in a wet scenario and dry scenario, respectively. The estimated PGA for the 2% probability of exceedance in 50 years is about 0.48 g and for 10% it is about 0.3 g, closer to the current design PGA in the Nepalese building code (NBC 2020).
An important geotechnical aspect is the superficial geology, the liquefiable layers are due to the presence of the river (supported by the GEER evidence, Hashash et al. 2015). However, when considering the distribution of the liquefaction potential in Fig. 8d in the central Valley, most areas correspond with the Somnez designation 'moderate' when located adjacent to the river edge. Two boreholes located between Kathmandu and Lalitpur either side of the river help evidence this result, and this probably is due to the dominant silt and clay-like materials often present at depth at these locations. The spatial position of these points (and the kriging results) gives lower values of potential liquefaction. As this indicates the 'dry scenario', the saturation in such deposits will be lower. Considering the laminated nature of the deposits and the fact that many locations are without borehole data, the results presented in this work are preliminary.
The flood plain areas have been identified and considered as having a high liquefaction potential used as a working assumption in all maps. The Gokarna and Tokha Formations at the northern part of the valley contain sand-dominant soil (Fujii and Sakai 2002 and Fig. 2). The Kalimati Formation dominantly comprises clayey silt has a lower liquefaction potential (Fujii and Sakai 2002). The liquefaction potential maps for all cases show that the northern part (Gokarna Formation) has a higher liquefaction potential than the southern (Kalimati Formation) region which complies with expectations considering the dominant constituents of these two materials. This result is expected given the geological nature of the deposits (the Kalimati is mainly clay while the Gorkarna is mainly sand). However, the original liquefaction map shown in Shrestha et al. (1998) (see Fig. 1a) does not follow the geological expectation in the same way as the analysis presented here, or that of Piya (2004) and Piya et al. (2004) when based upon on a database containing more recent ground investigations (Gilder et al. 2019b(Gilder et al. , 2020. No severe liquefaction was observed in the Kathmandu Valley during the Gorkha earthquake as discussed in previous studies (e.g., Chiaro et al. 2015;Moss et al. 2017). Based on the present study, this can be attributed to the season of the year in which the Gorkha earthquake occurred. April is peak dry season in the Kathmandu Valley (Fig. 8d). Most of the area in this season has a low potential for liquefaction, therefore, this result matches with the relatively limited evidence of liquefaction damage during that earthquake. If a similar, or larger, earthquake occurred in the future during peak wet season, the soil is expected to liquefy more significantly as shown in the Figs. 8a and c and 9a and c. 1 3

Summary and conclusions
Liquefaction potential zoning maps are useful tools for seismic hazard assessment. In this study, information compiled from geo-database SAFER/GEO-591 was employed to develop new maps of liquefaction potential using SPT data. Notwithstanding the additional information provided by the database, the area of the valley is still not well characterized from a geotechnical perspective and therefore interpolation by ordinary kriging was used to obtain continuous hazard maps of liquefaction potential, developed for different scenarios of hazard-consistent PGA. The following conclusions are drawn: (a) The effect of changing depth of the water table to simulate seasonal variation was studied which is shown to have a significant effect on the distribution of computed liquefaction potential. This confirms the observations made by Moss et al. (2017) and highlights the need for season-dependent liquefaction susceptibility studies. This is an important issue as it further affects the predictions of structural and infrastructure damage in Kathmandu valley, which are key elements of regional loss assessment. (b) As expected, the scenario of shallow water table typical of the monsoon season is characterized by higher calculated liquefaction potential with respect to the dry season scenario. (c) The Gokarna Formation appears to have the highest computed potential for liquefaction with respect to other geological formations studied, which has resulted in maps that indicate higher liquefaction potential in the north of the valley compared to the south (where the composition is more cohesive).
To further refine the above observations, site response analyses at the city level can be performed to calculate the cyclic stress ratio in a more refined manner (De Risi et al. 2019). Currently the liquefaction potential maps are reliant on the available borehole distribution, and it should be noted that some areas are currently not well characterized (e.g., Bhaktapur). It is also expected that the assessment of liquefaction potential of the southernmost valley may increase with data from further investigations if the area is underlain by both weathered fan and deltaic deposits (Sakai et al. 2016). More recent work on liquefaction potential has investigated the role that silts might have on liquefaction potential (Shuttle and Cunning 2007). This may inform further work which may benefit future liquefaction potential studies for the Kathmandu Valley, given the central, most populated parts of the valley are underlain by potentially loose, saturated silts. Further work is also needed to compare the exact locations of observed liquefaction against the results predicted in this work. However, this study has shown the value of the SAFER/GEO-591 (Gilder et al. 2019b) database for regional estimates of liquefaction potential which may be useful for planning and loss assessment purposes.  Table 6) [Photo: RM Pokhrel]

Fig. 12
Tilted building due to liquefaction at Imadol (Liq. ID 6 in Table 6) [Photo: RM Pokhrel] Table 6) [Photo: RM Pokhrel] Funding The authors acknowledge the support from the Engineering and Physical Science Research Council (EPSRC) project 'Seismic Safety and Resilience of Schools in Nepal' SAFER (EP/P028926/1). The second author acknowledges the support of EPSRC (EP/R51245X/1).

Conflict of interest
The authors declare that they have no conflict of interest.
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