GIS-Based Landslide Susceptibility Mapping for Land Use Planning and Risk Assessment

: Landslide susceptibility mapping is essential for a suitable land use managing and risk assessment. In this work a GIS-based approach has been proposed to map landslide susceptibility in the Portoﬁno promontory, a Mediterranean area that is periodically hit by intense rain events that induce often shallow landslides. Based on over 110 years landslides inventory and experts’ judgements, a semi-quantitative analytical hierarchy process (AHP) method has been applied to assess the role of nine landslide conditioning factors, which include both natural and anthropogenic elements. A separated subset of landslide data has been used to validate the map. Our ﬁndings reveal that areas where possible future landslides may occur are larger than those identiﬁed in the actual ofﬁcial map adopted in land use and risk management. The way the new map has been compiled seems more oriented towards the possible future landslide scenario, rather than weighting with higher importance the existing landslides as in the current model. The paper provides a useful decision support tool to implement risk mitigation strategies and to better apply land use planning. Allowing to modify factors in order to local features, the proposed methodology may be adopted in different conditions or geographical context featured by rainfall induced landslide risk.


Introduction
Landslides are among the most hazardous natural instability processes, which globally lead enormous socio-economical losses and damage to property every year [1][2][3][4]. Shallow landslides and debris flows represent one of the major causes of destruction to structures and infrastructures, injured people and casualties in mountain and hilly regions: they are usually triggered by short and severe rainfalls. Shallow landslides generally involve small volumes, unlike debris flows. However, both can be extremely damaging due to their widespread spatial distribution across territories, rapid development and high velocity of propagation [5].
According to Varnes [6], landslide risk can be defined as the probability of the occurrence of a potentially damaging landslide in a given area and for a defined period of time. Hazard assessment requires the estimation of the landslide magnitude, temporal frequency and spatial location [7]. The affectable area and recurrence time are complicated to predict because they are correlated to the complex natural processes that control the mass movement and the difficulty in raising historical landslide data respectively. Surely it could be easier to confine their predictive models to single slopes or very small areas for which detailed physical parameters and historical records can be found. On the other hand, the spatial distribution of potentially unstable areas can be easier to predict by assessing the likelihood of landslide occurrence in a region on the basis of the local ground conditions [8]. Therefore, assessing landslide susceptibility represents the first step in evaluating landslide risk management. Our study aims to highlight the difference between the two susceptibility models and how a recurrent spatial analysis of landslide distribution at local scale is essential to update the knowledge of the areas where shallow landslides and debris flows may occur in the future, so that the most effective land management and successful prevention of landslide risk can be provided. Further, including anthropogenic factors in conditioning corresponds to the added effects of human activity on the Earth's surface, which considers man as a morphogenetic factor. The effects of human modification, that may assume a very high importance locally, may result even in landslide generation. In this sense the diffuse presence of abandoned man-made terraces may result in a possible source of shallow landslides.

Study Area
The Portofino Promontory extends for 23 km 2 in the eastern Liguria, Northern Italy, between Genoa Gulf (W) and Tigullio Gulf (E) (Figure 1). It is world-famous for the attractive landscapes and seascapes and its natural, historical and cultural heritage. Wellknown settlements of great value and seaside resorts stand along its coast, such as Camogli, San Fruttuoso, Portofino, Paraggi and Santa Margherita Ligure. Because of the great environmental and cultural values, the promontory is protected and included in the Regional Natural Park of Portofino (18 km 2 ) since 1935, including the seaward area that became a marine reserve in 2001, when the boundaries of the protected area have been redefined. The geological setting of the promontory is made by a sedimentary rock masses, with conglomerate and flysch [40,41]. The Conglomerate of Portofino (Oligocene) crops out in the southern sector, particularly along the steep slopes and high cliffs between Punta Chiappa and Portofino, and secondarily along the south-eastern coastal stretches, between Portofino and Punta Cervara. Conglomerate is made up of heterogeneous clastic The geological setting of the promontory is made by a sedimentary rock masses, with conglomerate and flysch [40,41]. The Conglomerate of Portofino (Oligocene) crops out in the southern sector, particularly along the steep slopes and high cliffs between Punta Chiappa and Portofino, and secondarily along the south-eastern coastal stretches, between Portofino and Punta Cervara. Conglomerate is made up of heterogeneous clastic elements, mainly of marly limestone, sandstone, limestone and secondarily of other lithotypes, in a sandy-limestone matrix. The formation features a fragile deformation tectonic, with several fault and fracture systems oriented mainly NW-SE and NE-SW, both at the mesoand macro-scale [42]. The Flysch of Mt. Antola (Cretaceous Sup. -Paleocene) is made up of marly limestone layers ranging in thickness from decimeters to meters, with shales, siltstones and calcarenites interlayers. It forms the central and norther sectors of the promontory and widely crops out along the western slopes between Scogli Grossi and Castellaro. The formation has been involved in a complex polyphase deformation tectonic, both ductile and fragile, with large-scale folds with SSW vergence and WNW-ESE axis orientation [43,44] which are well exposed along the cliffs.
Several fracture and direct fault systems, with different directions, control both geological and morphological settings of the promontory. The drainage pattern and the coastline and ridge orientation are the result of the extensive tectonic activity that affected the Ligurian continental margin during the Quaternary [45,46].
The peculiar geological and morphological setting is responsible for the widespread instability processes, which affected large portions of the promontory, locally caused by erosional processes and undercutting produced by running water and sea wave action along slopes and cliffs. Most of the mass movements developed along the contact between the formations, due to the different geomechanics behavior: the two largest landslides are quite close to the tectonic contact, at Le Gave (eastern sector) and San Rocco (western sector) [47][48][49] (Figure 2A,B). Rockfalls and shallow landslides, including rapid and destructive mud and debris flows, are involved frequently in the southern steep sectors shaped in the conglomerate, whereas landslides characterized by different movement types, including sliding and complex landslides, affected the gentler slopes shaped in the marly limestone flysch [50,51] (Figure 2C,D). Recurrent falls and topples occurred along the high cliffs made up of both conglomerate and flysch, also favored by the sea wave action generally triggered by SW (Libeccio, dominant) and SE (Scirocco, prevailing) winds depending on the orographic orientation ( Figure 2E,F).
Mountains with high elevations (up 600 m a.s.l.) close up the coastline and high cliffs (up to 200 m) characterize the southern and western sectors: slopes face mainly from SE to W, with high to very high steepness values ranging from 50% to 75%, which locally exceed 75% along the cliffs. Whereas the eastern and northern sectors of the promontory are featured by gentle hills, with prevalently E-and NE-facing slopes and steepness values ranging generally from 10% to 50%. A very small coastal floodplain (<0.5 km 2 ) occupies the final stretch of San Siro, Magistrato and Santa Barbara Creeks, where the town of Santa Margherita Ligure stands ( Figure 1).
Catchments have a high slope gradient, and they are generally small to very small in size (less than 1 km 2 ), except for few of them which extend up to 5 km 2 (Acqua Morta and San Siro creek, Gentile stream and the upper Boate stream basin). Consequently, their hydrologic response to rainfall events is quite rapid, with time of concentration typically less than 1-2 h. Watercourses are generally short, steep and incised, with a typical angular pattern, as a result of the high relief and tectonics control. Streams are frequently dry, particularly in summer months or during prolonged dry spell; however, during heavy rainfall events, they can reach more considerable discharges with a large solid transport, thereby evolving into rapid mud or debris flows.
Forests (950 ha) and shrub and/or herbaceous vegetation association (200 ha) occupy large sectors of the promontory. Forested areas include broad-leaved forests (640 ha), coniferous forest (124 ha) and mixed forest (186 ha). High cliffs and the steep S-facing slopes have little or no vegetation (75 ha), followed by sparse vegetation (58 ha), bare rocks (15 ha), whereas small pebbly beaches are in the little bays (<2 ha). The northern and eastern hilly sectors are largely occupied by permanent crops (667 ha), including olive groves (665 ha) and vineyards (<2 ha), heterogeneous agricultural areas (21 ha), pastures (2 ha) and arable lands (<1 ha). Terraces characterize large sectors of the Portofino promontory, totally modifying the former natural landscape: they are widespread both in the current agricultural lands, largely represented by olive groves, in use or abandoned, and in re-vegetated areas or in totally abandoned ones [51]. Artificial areas represent a very small portion of the territory: urban fabric (247 ha), industrial, commercial and transport units (32 ha) and artificial, non-agricultural vegetated areas (33 ha) occupy small stretched of the coastal slopes and floodplain. shaped in the conglomerate, whereas landslides characterized by different movement types, including sliding and complex landslides, affected the gentler slopes shaped in the marly limestone flysch [50,51] (Figure 2C,D). Recurrent falls and topples occurred along the high cliffs made up of both conglomerate and flysch, also favored by the sea wave action generally triggered by SW (Libeccio, dominant) and SE (Scirocco, prevailing) winds depending on the orographic orientation ( Figure 2E,F). The complex geological, climate and environmental history and setting contribute also to a significant spatial pedological variability in the soil horizons of the Portofino promontory with six different Reference Soil Groups [52] and evidence of an extensive ancient erosional surface and several paleosol features, suggesting the existence of different tectonic and climate conditions that have been responsible for erosion phenomena [53].
The climate of the Portofino promontory is conditioned by the local orographic configuration: the presence of a mountain relief which exceed 600 m close to the sea (<1 km) and the slopes aspects, determine peculiar insolation and exposure conditions to marine winds, with a significant spatial climate variability. The climate is Mediterranean, with hot and dry summers and mild winters in the southern, and changeable, rainy weather; whereas a midhill zone, with more abundant precipitations and colder winters, characterizes the northern sectors. Regime rainfall ranges depending on the orographic setting, with maximum rainfall in autumn, and minimum rainfall in summer [54]. Intense and short duration rainfalls frequently occur in late summer or autumn months, from August to November, generated by a typical atmospheric circulation over the Genoa Gulf, called Genoa Low [55,56] usually associated with intense thunderstorms [57]: the resulting convective systems generate localized and severe precipitation, which are frequently responsible for flash floods and widespread shallow landslides and mud-debris flows [51,58,59].

Data and Research Methodology
A catalogue of rainfall-induced rapid and very rapid mass movements occurring in the study area since 1910 has been compiled. In particular, gravitational processes with high to very high velocity of the movement of variable volumes of materials triggered by rainfall events, including shallow landslides, mud or debris flows and rock falls, were considered. Information was gathered from different sources, including scientific papers, technical reports, archives of local municipalities and newspaper articles [59]. Most of the historical data derive from the inventory of sites historically affected by landslides and floods events in Italy in the period 1918-1994 of the AVI Project (Hit Areas of Italy) of GNDCI-CNR (National Group for Geo-hydrological Disaster Protection of National Research Council) [60].
Using regional base maps at 1:10,000 scale (Table 1), landslides have been georeferenced within a GIS Geographical Information System open source software (QGIS 3.10). Since areal information on landslide size has been difficult to retrieve due to the heterogeneous source types, punctual features have been adopted, which represents the highest point of the landslide scarp. Simultaneously, for each landslide feature the following information has been recorded [59]: (i) landslide type [5,61]; (ii) geographical location and its spatial accuracy, from P1 (approximative location of slope failure within a buffer area < 1 km 2 ) to P3 (buffer area > 10 km 2 ); (iii) data of the landslide occurrence; (iv) source of landslide information and/or archive where bibliographic research was carried out.
In addition to the past rainfall-induced landslides inventory, the set of thematic maps listed in Table 1 has been used to analyze the correlation between slope failures and both natural and anthropic predisposing factors, and to generate the landslides susceptibility map of the study area.

Landslide Conditioning Factors
Rainfall is commonly recognized as the major landslide causative elements [65]: shallow landslides and mud-debris flows triggered by very short, but intense or prolonged, rainfalls can be particularly destructive due to their spatial distribution and rapid propagation. However, several natural factors control the slope stability, including lithology, Land 2021, 10, 162 7 of 28 topography, hydrographical network, land use and geomorphological processes can affect the initiation of slope failures. Several researches highlighted the relationship between shallow landslides occurrence and human activities [66][67][68][69]: deforestation for farming, modifications in drainage patterns and slope profile due to artificial road cuts, fills or other construction purposes, reduce the rainfall infiltration and increase the erosional processes by surface run-off, predisposing slope to collapse.
In order to assess the landslide zonation of the Portofino promontory, the spatial relationships among the rainfall-induced rapid mass movements that occurred in the study area from 1910 to 2019 have been analyzed, and natural and anthropic landslide conditioning factors have been selected. In particular, the following nine thematic variables have been selected: (i) lithology, (ii) slope aspect, (iii) slope acclivity, (iv) land use, (v) terraced landscape, (vi) hydrographic elements distance, (vii) distance to man-made cuts elements, (viii) distance to man-made structures and (ix) existing gravitational processes ( Table 2).

Lithology
It is generally known that geological and structural settings can affect the initiation and development of shallow landslides [70,71]. We considered five classes derived from the thematic regional map at 1:10,000 scale (Table 1) and based on the lithological features ( Figure 3A): (i) heterogeneous clayey and sandy materials, which form the alluvial deposits; (ii) incoherent soils, including silt and clay with granular fraction and coarse soils, which form the thick slope covers); (iii) heterogeneous materials of anthropic origin, which include fills and artificial deposits; (iv) marly limestone and marls (Flysch of Monte Antola) and (v) conglomerate (Conglomerate of Portofino), with eluvial and colluvial deposits.

Slope Aspect
Among morphological factors, aspect plays a relevant role in slope stability, inducing different conditions of insolation, temperature, land cover, weather conditions and rainfall exposure and, therefore, controlling important properties of the soils, e.g., temperature, moisture and level of saturation [28,72]. Landslide occurrence is more common on southfacing slopes than on north slopes, where failures occasionally occur due to the presence of more vegetation covers that can increase soil strength and reduce water infiltration [73,74]. Adopting the regional thematic map at 1:10,000 scale (Table 1), we considered the nine aspect classes shown in Figure 3B.

Slope Acclivity
Acclivity plays also a relevant role in the activation of instability processes [75,76]. We derived the topographical information from the regional technical map at 1:10,000 scale (Table 1), where slope steepness (in percentage) has been organized in seven classes, from 0 to 10% to >100% ( Figure 3C).

Land Use
Several studies highlighted the relevant role of land use and changes in land use in triggering shallow landslide [67,77], in addition to the other geological and morphometric predisposing factors. We used the regional land use map at 1:10,000 scale based on the CORINE nomenclature [62]. In particular, we considered ten land use categories of second level ( Figure 3D): (i) urban fabric, (ii) industrial, commercial and transport areas, (iii) artificial, non-agricultural areas, (iv) arable land, (v) permanent crops, (vi) pastures, (vii) heterogeneous agricultural areas, (viii) forests, (ix) shrubs and/or herbaceous vegetation association and (x) open spaces with little or no vegetation, including beaches and bare rocks.
Land 2021, 10, 162 9 of 28 CORINE nomenclature [62]. In particular, we considered ten land use categories of second level ( Figure 3D): i) urban fabric, ii) industrial, commercial and transport areas, iii) artificial, non-agricultural areas, iv) arable land, v) permanent crops, vi) pastures, vii) heterogeneous agricultural areas, viii) forests, ix) shrubs and/or herbaceous vegetation association and x) open spaces with little or no vegetation, including beaches and bare rocks.

Terraced Landscape
Several studies have investigated the role of terraced landscapes in slope stability. One hand, cultivated terraces control runoff processes on steep slopes, erosion and rainfall infiltration, reducing the geo-hydrological risk; as a consequence, progressive terrace abandonment may affect negatively the stability of the slope in response to very intense rainfall events [78][79][80][81]. On the other hand, recent studies highlighted how the growth of natural vegetation on abandoned terraces increases the slope stabilization and, at the same time, how rainfall-induced shallow landslides affected both vegetated abandoned and well-maintained cultivated terraces [51,82,83]. Unlike authors who did not compute terraces in landslide susceptibility estimation [36], we included terraced landscape among the anthropic variables that may influence the shallow landslides initiation. Terraced surfaces in the study area are shown in Figure 4A: they have been detected carrying out the semi-automatic technique [51] for the terrace identification in the portion of Portofino promontory within the Natural Park boundaries, using the raster data listed in Table 1.  Retaining walls.

Existing Gravitational Processes
We also considered the presence of pre-existing landslides, which may represent areas with a potential higher proneness to slope instability. These instability processes derived from the regional catalogue of landslides at 1:10,000 scale [63] (Table 1), in which landslides are mapped and classified on the basis of type of movement and state of activity. In particular, we considered four classes: i) active/reactivated/suspended landslides, ii) dormant landslides, iii) inactive/stabilized landslides, and iv) area affected by widespread shallow landslides. In stable areas, certainly or supposed, we set two further classes based on a buffer zone of 50 m from the boundaries of mapped landslides ( Figure 5A).

Hydrographic Elements Distance
Proximity to hydrographic networks, including watercourses and springs, may affect the slope stability [33,34,84]. Morphological modifications due to gully erosion may influence the removal of incoherent materials and the activation of mass movements, particularly along steep slopes [85]; furthermore, watercourses may affect the slope stability by saturating the lower part of geomaterial and increasing the water level, particularly in cases of permeable bedrock due to lithological or mechanical properties. We derived watercourses and springs in the Portofino promontory from the regional thematic map at 1:10,000 scale (Table 1). To analyze their effects on shallow landslides triggering, we produced a buffer map where streams and springs are buffered at distance of 10 m ( Figure 4B).

Man-Made Cuts and Structures Distance
Similarly, anthropogenic changes to slope profile and runoff network induced by cutand-fill works can modify the stress-strain and drainage conditions, modifying the slope equilibrium and increasing the possibility of shallow landslides activation [86][87][88]. Slope cuts, such as roads or trails segments, frequently represent the source of failure [33,89,90]; but they can also act as a barrier or a preferential flow-path route, cutting the natural drainage network. The influence of road and trail networks distance on shallow landslide was analyzed, setting a buffer zone of 5 m around the linear elements ( Figure 4C). In particular, we considered both main and minor road features, extracted from the regional topographical database, and the trail network of the Portofino promontory derived from the correlate regional technical map (Table 1).
To analyze the influence of man-made structures distance on landslide occurrence, we extracted buildings, manufacts and retaining walls from the regional topographical database (Table 1) and buffered the features at a distance of 10 m ( Figure 4D).

Existing Gravitational Processes
We also considered the presence of pre-existing landslides, which may represent areas with a potential higher proneness to slope instability. These instability processes derived from the regional catalogue of landslides at 1:10,000 scale [63] (Table 1), in which landslides are mapped and classified on the basis of type of movement and state of activity. In particular, we considered four classes: (i) active/reactivated/suspended landslides, (ii) dormant landslides, (iii) inactive/stabilized landslides, and (iv) area affected by widespread shallow landslides. In stable areas, certainly or supposed, we set two further classes based on a buffer zone of 50 m from the boundaries of mapped landslides ( Figure 5A).

Analytic Hierarchy Process (AHP)
To assess the landslide susceptibility of the Portofino promontory combining all the variables, we adopted the Analytic Hierarchy Processes (AHP) developed by Saaty [91], a semi-quantitative multi-criteria decision-making approach which enables to compute rank and weight of each criterion by a pair-wise comparison.
This approach includes several steps: i) break a composite unstructured problem

Analytic Hierarchy Process (AHP)
To assess the landslide susceptibility of the Portofino promontory combining all the variables, we adopted the Analytic Hierarchy Processes (AHP) developed by Saaty [91], a semi-quantitative multi-criteria decision-making approach which enables to compute rank and weight of each criterion by a pair-wise comparison.
This approach includes several steps: (i) break a composite unstructured problem down into its component factors n and arrange them in a hierarchic order; (ii) assign numerical values according to the subjective relevance of each factor to determine its relative importance by a matrix-based pair-wise comparison where i, j = (1, 2, . . . , n); (iii) synthesize the rating to determine the priority ω n , i.e., the weight, to be assigned to each factor computing the normalized principal eigenvector λ max , which corresponds to the largest eigenvalue [92,93]. In the pair-wise comparison, a scale of preference alternatives is used to associate a score based on the subjective judgment on the relative importance of each factor against every other one (Table 3). Table 3. Scale of preference between two criteria used in the pair-wise comparison in AHP [88]. In this study, the nine considered variables influencing shallow landslides represent the component factors of the unstructured composite problem required by the method. To analyze the correlations between the conditioning factors and the landslides that occurred in the study area and arrange them in a hierarchic order, we firstly performed a simple frequency distribution analysis for each conditioning factor and for the different classes within each of them (Table 2). For this purpose, according to Chung and Fabbri [94] and Carrara et al. [95], we considered a portion of the gathered landslide inventory to evaluate the proneness to shallow landslide (training set), using the remaining landslides data to validate the resulting susceptibility model (test set) ( Figure 5B). The training set has been defined by selecting randomly [9] 80% of the georeferenced landslides with a geographical accuracy <10 km 2 (P1 and P2).

Degree of Preference Description
Next, with respect to their impact on slope stability, we performed the pair-wise comparison for each conditioning factor and for the different classes within each factor using the AHP Excel template [96]. The template, which works under Excel version MS Excel 2013, can solve and combine the matrix of pair-wise comparisons of a maximum number of ten criteria computed by a maximum number of twenty experts. In this work, we used this approach to combine AHP results computed by five participants. The AHP Excel template includes (i) twenty input worksheets for pair-wise comparisons, where priorities are calculated using the row geometric mean method (RGMM); (ii) a sheet for the consolidation of all judgments, where weights given in the input sheets by individual par- Final results include (i) weights of all considered criteria and associated errors (in %); (ii) principal or largest eigenvalue λ max of the matrix, and (iii) a modified consistency ratio CR as proposed by Alonso and Lamata [97], calculated in all input sheets and in the summary sheets. The consistency ratio CR is an index ranging from 0 to 1, used to determine the degree of matrix consistency; it has been defined by Saaty [92] as the ratio between the calculated consistency index of the matrix CI and a random consistency index RI.
The consistency index CI estimates the consistency of weights and ratings and it is calculated based on Saaty's [98] expression: where λ max is the largest eigenvalue and n is the order of the matrix, corresponding to the number of parameters. The random consistency index RI, reported by Saaty [92] as the average of the resulting consistency index depending on the order of the matrix, in the AHP Excel Template adopted in the present study is calculated using the Alonso and Lamata linear fit [97], which estimates the RI as the best adjustment fit of the values of -;λ max (n): where -;λ max is the mean of λ max . The CR is therefore calculated by the following expression: Value of CR smaller than or equal to 0.1 (10%) is acceptable and, consequently, the matrix is consistent.
An AHP consensus indicator S* is also calculated to quantify the consensus of the group, i.e., to estimate the agreement on the outcoming priorities between all the experts and it can be interpreted as a measure of overlap between priorities of the group members. This indicator is calculated using the partitioning diversity in Alpha and Beta diversity [99] derived from the Shannon entropy [100]. The consensus indicator S* ranges from 0% (no consensus between experts) to 100% (full consensus between experts): values below 50% indicate a very low consensus, i.e., a high diversity of judgments, whereas values ranging from 80% to 90% indicate a high overlap of priorities and an excellent agreement of judgments from the group members.

Landslide Susceptibility Map
Once coherent weights have been assigned to each landslide causal factor and to each class within conditioning factor performing the AHP approach, all thematic vector layers have been converted into grid format with a 5 × 5 m cell size using the GRASS 7 (Geographic Resources Analysis Support System) native plugin in QGIS. Next, the reclassification of all grid data by weight values has been performed using the SAGA (System for Automated Geoscientific Analysis) reclassify values algorithm in QGIS.
A raster analysis has been performed to construct the landslide susceptibility map (LSM) using the Raster Calculator tool in QGIS. All the weighted predisposing factors and their classes have been combined using a weighted linear sum and then normalized by scaling values between 0 and 1 using the maximum value for the calculated variable: where w ij is the weight factors of the class i in the conditioning factors j, W j is the weight of the landslide conditioning factor j. Lastly, values resulting from the raster analysis have been classified into 5 classes (low, moderate, high and very high) based on the histogram classification to determine the interval of each landslide susceptibility class in the map.

Results
We identified 85 rainfall events and 114 landslides in the 1910-2019 period. More than 50% of the observed instability processes involved the western and south-western sectors of the promontory, within the Camogli municipality, followed by Santa Margherita Ligure (30%) and Portofino (16%) ( Figure 6A). Shallow landslides (43%) and rock falls (30%) are the most representative type of rainfall-induced rapid mass movements. Debris and mud flows occur with less frequency (<10%) ( Figure 6B). Results of the landslides spatial analysis show that slope failures occurred mainly in marly limestone with shale interlayers (48%) and conglomerate (41%), whereas incoherent soils and heterogeneous materials of anthropic origin are involved less frequently (8% and 3% respectively). With respect to the morphometric parameters, mass movements induced by rainfall affected mainly slopes of east (21%), north-west (20%) and west (18%) direction; south-west (13%) and north-east (11%) are also relevant slope directions, whereas north and south-east directions (5% respectively) are no representative. Landslides triggered mainly on slopes with high and very high steepness values (70%), higher than 50%. Most of instability processes developed within vegetated areas, characterized by mixed forests (26%), olive groves (26%) and broad-leaved forests (20%). Regarding urbanized areas, landslides have been detected largely on slopes with a discontinuous urban fabric (15%). Only 1% of gravitational processes involved bare rocks. Half of the observed landslides affected terraced slopes (50%), made of dry-stone walls terraces or grassy embankments, both well-maintained and abandoned.
With respect to the existing landslides mapped in the regional master plans, we found that most of the rainfall-induced failures (80%) involved slopes where no landslides have been previously detected. Only in 20% of cases, they match with existing landslides, classified as active/reactivated/suspended (16%) and dormant (4%); this percentage increases to 45% if we consider a buffer of 50 m around the landslide features. Similarly, in few cases landslides occurred within 10 m from watercourses (11%) or within 5 m from man-made cuts and structures, including main roads (9%), trails (11%), buildings (21%), manufacts (7%) and retaining walls (27%).
Among the 114 landslides, we considered 102 processes for which geographical location was known with a high or medium spatial accuracy (P1 and P2). The training set used to assess the landslide susceptibility consists of 81 landslides.
As proposed by the AHP method, the pairwise comparison matrix has been constructed both between the nine landslide causal factors and between the classes within each of them. In order to assess their impact on slope stability, each variable has been rated against every other by assigning a relative dominant value between 1 and 9 to the intersecting cell based on the results of the frequency analysis performed using the random selected landslide training set. Table 4 summarizes normalized principal eigenvectors and associated errors for conditioning factors. Complete pairwise comparison matrixes for causal factors and for the classes within each landslide conditioning factor are shown in Appendix A, Appendix B and Appendix C. Results of the landslides spatial analysis show that slope failures occurred mainly in marly limestone with shale interlayers (48%) and conglomerate (41%), whereas incoherent soils and heterogeneous materials of anthropic origin are involved less frequently (8% and 3% respectively). With respect to the morphometric parameters, mass movements induced by rainfall affected mainly slopes of east (21%), north-west (20%) and west (18%) direction; south-west (13%) and north-east (11%) are also relevant slope directions, whereas north and south-east directions (5% respectively) are no representative. Landslides triggered mainly on slopes with high and very high steepness values (70%), higher than 50%. Most of instability processes developed within vegetated areas, characterized by mixed forests (26%), olive groves (26%) and broad-leaved forests (20%). Regarding urbanized areas, landslides have been detected largely on slopes with a discontinuous urban fabric (15%). Only 1% of gravitational processes involved bare rocks. Half of the observed landslides affected terraced slopes (50%), made of dry-stone walls terraces or grassy embankments, both well-maintained and abandoned.
With respect to the existing landslides mapped in the regional master plans, we found that most of the rainfall-induced failures (80%) involved slopes where no landslides have been previously detected. Only in 20% of cases, they match with existing landslides, classified as active/reactivated/suspended (16%) and dormant (4%); this percentage increases to 45% if we consider a buffer of 50 m around the landslide features. Similarly, in few cases landslides occurred within 10 m from watercourses (11%) or within 5 m from man-made cuts and structures, including main roads (9%), trails (11%), buildings (21%), manufacts (7%) and retaining walls (27%).
Among the 114 landslides, we considered 102 processes for which geographical location was known with a high or medium spatial accuracy (P1 and P2). The training set used to assess the landslide susceptibility consists of 81 landslides.
As proposed by the AHP method, the pairwise comparison matrix has been constructed both between the nine landslide causal factors and between the classes within each of them. In order to assess their impact on slope stability, each variable has been rated against every other by assigning a relative dominant value between 1 and 9 to the intersecting cell based on the results of the frequency analysis performed using the random selected landslide training set. Table 4 summarizes normalized principal eigenvectors and associated errors for conditioning factors. Complete pairwise comparison matrixes for causal factors and for the classes within each landslide conditioning factor are shown in Appendices A-C. Calculated weights for the landslide conditioning factors range between 0.031 and 0.311: getting the highest value, slope acclivity represents the most relevant factor in the initiation of shallow landslides on the Portofino promontory, followed by land use (0.197) and lithology (0.155). Contrariwise, distance from hydrographic elements and man-made cuts slightly influence the landslide occurrence, weighting 0.034 and 0.031 respectively. By considering the different classes within each conditioning factor (Appendices B and C), the lithological features more predisposing to instability are limestone flysch (0.507) and conglomerate (0.308), whereas low weights have resulted for incoherent soils (0.04) and heterogeneous materials of anthropic origin (0.022). Regarding the morphometric conditioning factors, the highest weights have been assigned to slopes facing NW (0.285) and E (0.248) respectively and slope acclivity values ranging between 51% and 75% (0.331); medium weights to slope oriented to W (0.144) and SW (0.111) and steepness range values ranging from 76% to 100% (0.221) and higher 100% (0.202) respectively; lowest weights to the remaining morphometric classes. For land use, forest (0.358) is the more predisposing class to shallow landslides initiation, followed by permanent crops (0.204) and urban fabric (0.150); similarly, presence of terraces greatly influences the landslides occurrence (0.739). Weights result proportionally to the distance of landslides from the hydrographic network (0.394), man-made cuts (0.672) and anthropic structures (0.540): the farthest buffer zones had the higher assigned weights. Regarding pre-existing landslides, the highest scores have been assigned to area where no former gravitation processes have been mapped within the buffer zone higher (0.423) and lower (0.300) than 50 m from the existing landslide boundaries.
Consistency of the weights and rating calculated for each conditioning factors and the agreement on the outcoming priorities between all the participants are shown in Table 5. Values of the Consistency Ratio index (CR) are smaller than 10%, confirming that all the constructed matrixes are consistent: excepting for lithology (9.2%), CR values range from 0.0% (presence of terraced areas) to 5.2% (presence of existing landslides). Consensus indicator (S*) values reported in Table 5, ranging from 94.6% and 99.0%, show a very good consensus between the members of the research team.
Combining weightage of conditioning factors and their classes, we obtained the landslide susceptibility map of the Portofino promontory. We normalized the resulting LSM values, which ranged from 0.079 to 0.401, by scaling values between 0 and 1. In order to determine the class intervals in the obtained map, we took into consideration the classification systems commonly applied in landslide susceptibility zonation: natural breaks, quantiles and equal intervals [101]. On the basis of the raster map histogram, which is multimodal and shows empty class intervals, we adopted the natural breaks method to divide the LSM values into five classes shown in Table 6. In this case, the quantile Land 2021, 10, 162 16 of 28 classification is not appropriate because data are not linearly distributed; whereas the lowest susceptibility class is too emphasized relative to others using equal intervals. The resulting landslide susceptibility map for the Portofino promontory is presented in Figure 7A. Most of the territory (74%) results prone to shallow landslide occurrence: the highest extension percentage (30%) falls into moderate landslide susceptibility class, followed by high (26%) and very high (18%) susceptibility classes ( Figure 7B). Otherwise, a small portion of the study area (26%) has been classified with low and very low landslide susceptibility.
We observed that areas with the highest proneness to rapid and very rapid mass movements occurrence (class = 5) comprise primarily the southern sectors of the promontory, where bedrock mainly consists of flysch (57%) and, secondarily, of conglomerate (30%), and slopes have a prevalent E (21%) and SE (14%) exposure, with high and very high steepness values (43%) comprised between 51% and higher than 101%. Sectors with high to very high landslide susceptibility are largely covered by forests (45%), permanent crops (34%) and shrubs or other natural vegetation (11%), with large areas characterized by outcropping bedrock, particularly along the high cliffs. Furthermore, they show the lowest interaction with anthropic elements, including roads (12%), buildings (6%), man-made structures (5%) and terraces (7%), and with pre-existing gravitational processes (1%).
Validation of the landslide susceptibility map has been performed on the basis of the test set consisting of 20 randomly selected landslide locations [94]. The distribution of landslides in the five LSM classes represents the qualitative assessment of the susceptibility map: we found that most of the landslides (65%) fell within the very high and the high susceptibility classes (35% and 30% respectively), confirming the strong connection between the occurrence of rainfall-induced rapid mass movements and the produced susceptibility zonation. A quantitative assessment of the predictive accuracy of the map has been computed using the Receiver Operating Characteristic curve (ROC) and the Area Under Curve (AUC) [35,102]. For this purpose, we plotted the true positive rate (TPR), i.e., the correctly predicted events, opposite to the false positive rate (FPR), i.e., the falsely predicted events, by varying the cut-off value. The prediction curve shows that the AUC value was 0.73 ( Figure 8). According to Sewts [103], the quantitative relationship between the AUC value and the accuracy of the predictive model is classified as weak (0.5-0.6), moderate (0.6-0.7), good (0.7-0.8), very good (0.8-0.9) and excellent (0.9-1.0). Therefore, the proposed We observed that areas with the highest proneness to rapid and very rapid mass movements occurrence (class=5) comprise primarily the southern sectors of the promontory, where bedrock mainly consists of flysch (57%) and, secondarily, of conglomerate (30%), and slopes have a prevalent E (21%) and SE (14%) exposure, with high and very high steepness values (43%) comprised between 51% and higher than 101%. Sectors with high to very high landslide susceptibility are largely covered by forests (45%), permanent crops (34%) and shrubs or other natural vegetation (11%), with large areas characterized by outcropping bedrock, particularly along the high cliffs. Furthermore, they show the lowest interaction with anthropic elements, including roads (12%), buildings (6%), man-made structures (5%) and terraces (7%), and with pre-existing gravitational processes (1%).
Validation of the landslide susceptibility map has been performed on the basis of the test set consisting of 20 randomly selected landslide locations [94]. The distribution of landslides in the five LSM classes represents the qualitative assessment of the susceptibility map: we found that most of the landslides (65%) fell within the very high and the high susceptibility classes (35% and 30% respectively), confirming the strong connection between the occurrence of rainfall-induced rapid mass movements and the produced susceptibility zonation. A quantitative assessment of the predictive accuracy of the map has been computed using the Receiver Operating Characteristic curve (ROC) and the Area Under Curve (AUC) [35,102]. For this purpose, we plotted the true positive rate (TPR), i.e., the correctly predicted events, opposite to the false positive rate (FPR), i.e., the falsely predicted events, by varying the cut-off value. The prediction curve shows that the AUC value was 0.73 ( Figure 8). According to Sewts [103], the quantitative relationship between the AUC value and the accuracy of the predictive model is classified as weak (0.5 -0.6), moderate (0.6 -0.7), good (0.7 -0.8), very good (0.8 -0.9) and excellent (0.9 -1.0). Therefore, the proposed landslide susceptibility map had a good prediction accuracy in rapid mass movements occurrence in the study area, when considering all the considered causative factors.

Discussion
The landslide susceptibility map obtained through the AHP semi-quantitative approach ( Figure 9A) represents a great tool for risk mitigation planning. The proposed methodology, already applied in similar geographical and geological context, combines

Discussion
The landslide susceptibility map obtained through the AHP semi-quantitative approach ( Figure 9A) represents a great tool for risk mitigation planning. The proposed methodology, already applied in similar geographical and geological context, combines an objective and quantitative component with a degree of subjectivity that arises from the experts' judgement, which are properly mediated through the AHP method. Then, the subjectivity level, although reduced in importance, allows one to introduce the experts' opinion in the decision-making process. The result is a susceptibility map that combines the experts' opinions and the objective record of past events. lithology where a statistical approach is used, considering the proportion of in landslide lithotype. Maps are summed up, and after normalization, susceptibility classes are assigned. Then, the methodology is highly affected by subjectivity and strongly relies on the presence of active and inactive landslides. Conditioning factors at local scale, including man-made landforms, are not included in the assessment of landslide susceptibility. Furthermore, areas where active, dormant or inactive/stabilized landslide, deep seated gravitational slope deformation, widespread active or dormant instability phenomena and shallow landslides are detected, are automatically classified as high or very high susceptibility zones. The obtained map is classed in 5 increasing levels of susceptibility, named from Pg0 to Pg4 ( Figure 9B). We observed that areas with very high landslides susceptibility overlap effectively with existing active mapped landslides; similarly, slopes with high susceptibility are largely affected by existing dormant or inactive landslide.
The comparison between the regional susceptibility zonation and the spatial distribution of rainfall-induced shallow landslides occurred in the Portofino promontory after 2013, which is the year of publication of the regional map, shows that most of them affected slopes classified as medium (Pg2) susceptibility. This result highlights the unreliability of the previous model to map landslide susceptibility for predicting areas where new slope failures may occur, as it probably relies too much on the existing phenomena in terms of their geometrical features, and less on the conditioning factors.
The differences between the previous model and the proposed one ( Figure 9) are particularly relevant in the southern part of the area, whose lithology is conglomerate, which is characterized by strong steepness. This factor, in the studied area, is probably the crucial one but it is primarily accompanied by man-made landforms and hydrographical network, and then by the others. The proposed model probably underestimates the presence of existing large landslides, but this apparent limitation may be easily overcome, adopting the same method of the actual in-use model, which automatically assigns the highest class to active landslide zones ( Figure 10). In fact, it is surely true that active landslides represent risk elements themselves and may result, in some local portions, as a possible source of rapid mass movements. Actually, the river basin management plan (defined Basin Master Plan) [104] adopts a different methodology to obtain the landslide susceptibility map ( Figure 9B). The methodology, which derives from a specific technical regulation, includes some conditioning factors at the catchment's scale: lithology, slope steepness, land use, hydrological effectiveness, soil cover and related granulometry and the presence of active or inactive landslides. Some other worsening factors are then included, e.g., lithological contact, fault, erosional talweg channel, edge of fluvial erosion scarp, terrace edge, slope angle discontinuity. Weights within every factor are assigned subjectively, apart from lithology where a statistical approach is used, considering the proportion of in landslide lithotype. Maps are summed up, and after normalization, susceptibility classes are assigned. Then, the methodology is highly affected by subjectivity and strongly relies on the presence of active and inactive landslides. Conditioning factors at local scale, including man-made landforms, are not included in the assessment of landslide susceptibility. Furthermore, areas where active, dormant or inactive/stabilized landslide, deep seated gravitational slope deformation, widespread active or dormant instability phenomena and shallow landslides are detected, are automatically classified as high or very high susceptibility zones. The obtained map is classed in 5 increasing levels of susceptibility, named from Pg0 to Pg4 ( Figure 9B).
We observed that areas with very high landslides susceptibility overlap effectively with existing active mapped landslides; similarly, slopes with high susceptibility are largely affected by existing dormant or inactive landslide.
The comparison between the regional susceptibility zonation and the spatial distribution of rainfall-induced shallow landslides occurred in the Portofino promontory after 2013, which is the year of publication of the regional map, shows that most of them affected slopes classified as medium (Pg2) susceptibility. This result highlights the unreliability of the previous model to map landslide susceptibility for predicting areas where new slope failures may occur, as it probably relies too much on the existing phenomena in terms of their geometrical features, and less on the conditioning factors.
The differences between the previous model and the proposed one ( Figure 9) are particularly relevant in the southern part of the area, whose lithology is conglomerate, which is characterized by strong steepness. This factor, in the studied area, is probably the crucial one but it is primarily accompanied by man-made landforms and hydrographical network, and then by the others. The proposed model probably underestimates the presence of existing large landslides, but this apparent limitation may be easily overcome, adopting the same method of the actual in-use model, which automatically assigns the highest class to active landslide zones ( Figure 10). In fact, it is surely true that active landslides represent risk elements themselves and may result, in some local portions, as a possible source of rapid mass movements. The comparison between the proposed susceptibility map ( Figure 10) and the regional susceptibility zonation ( Figure 9B) has been performed through Cohen's Kappa calculation [105,106], using the Map comparison kit software, version 3.2.3 [107]. The obtained Kappa value was 0.108, and the correct fraction was 0.308, showing a general slight concordance between the two maps. Results per susceptibility class are shown in Table 7: medium and high classes displayed the lowest and no concordance, respectively, while the very low one presented a relatively higher degree of concordance, confirming the general result even if differentiating between classes. The lowest susceptibility class corresponded substantially with the lower slope gradient areas, that is the lower values of the more critical conditioning factor. On the other hand, the weak concordance in the three higher susceptibility classes highlights the strong differentiation between the two maps where landslide triggering probability is higher. The comparison between the proposed susceptibility map ( Figure 10) and the regional susceptibility zonation ( Figure 9B) has been performed through Cohen's Kappa calculation [105,106], using the Map comparison kit software, version 3.2.3 [107]. The obtained Kappa value was 0.108, and the correct fraction was 0.308, showing a general slight concordance between the two maps. Results per susceptibility class are shown in Table 7: medium and high classes displayed the lowest and no concordance, respectively, while the very low one presented a relatively higher degree of concordance, confirming the general result even if differentiating between classes. The lowest susceptibility class corresponded substantially with the lower slope gradient areas, that is the lower values of the more critical conditioning factor. On the other hand, the weak concordance in the three higher susceptibility classes highlights the strong differentiation between the two maps where landslide triggering probability is higher. Table 7. Kappa per susceptibility class map comparison between regional zonation and the proposed one. Then, the proposed susceptibility map (Figure 10), modifying landslides area zonation, may be intended as a more effective and efficient tool to support risk mitigation strategies and planning. More accurate knowledge of where a future possible landslide may occur allows us to eventually reduce the importance of critical man-induced factors and to promote proper prevention measures that are crucial for reducing damage and even victims [39,108,109].

Conclusions
The research allowed us to assess a landslide susceptibility map for the Portofino promontory, based on over 110 years of rapid mass movements inventory and experts' opinions, to apply a semi-quantitative AHP method. Then, the methodology combines the quantitative approach with an expert-based view. The analysis of nine conditioning factors, which includes anthropogenic landforms related ones, results in a susceptibility map that highlights areas where possible future landslides may occur with a reliability that appears higher than the one of the actual officially adopted map. The way the proposed map has been compiled seems more oriented towards the possible future landslide scenario, rather than weighting the existing landslides with higher importance.
Then, the proposed map results as a possible decision support tool to implement risk mitigation strategies and to better apply land use planning in an area that is periodically hit by intense rain events that often induce rapid mass movements. The combination of those types of landslides and flash flood often occurs, causing the culverts saturation in urban and peri-urban areas and resulting in large damage. The RECONECT EU funded project is actually adopting risk mitigation strategies for slope stabilization in the studied area and a susceptibility map is a crucial decision support tool for interventions planning [110].
Finally, the methodology allows us to modify factors, including new ones or excluding others, in order to localize features, and it may then be adopted in different conditions or geographical contexts.

Appendix B
Summary of AHP analysis: pairwise comparison matrix computed by five participants, normalized principal eigenvector value and associated errors for the classes within each landslide conditioning factor.