Next Article in Journal
Investigation of Trace and Critical Elements (Including Actinides) in Flotation Sulphide Concentrates of Kassandra Mines (Chalkidiki, Greece)
Previous Article in Journal
Spatial and Temporal Variations in the Incidence of Dust Storms in Saudi Arabia Revealed from In Situ Observations
 
 
Search for Articles:
Title / Keyword
Author / Affiliation / Email
Journal
Article Type
 
 
Advanced Search
 
Section
Special Issue
Volume
Issue
Number
Page
 
Journals
Geosciences
Volume 9
Issue 4
10.3390/geosciences9040163
geosciences-logo
Submit to this Journal Review for this Journal Propose a Special Issue
► Article Menu

Article Menu

share Share announcement Help format_quote Cite question_answer Discuss in SciProfiles thumb_up
...
Endorse textsms
...
Comment
first_page
settings
Order Article Reprints
Font Type:
Arial Georgia Verdana
Font Size:
Aa Aa Aa
Line Spacing:
Column Width:
Background:
Article

GIS-Based Rockfall Susceptibility Zoning in Greece

by
Charalampos Saroglou
Department of Geotechnical Engineering, School of Civil Engineering, National Technical University of Athens, 15773 Athens, Greece
Geosciences 2019, 9(4), 163; https://doi.org/10.3390/geosciences9040163
Submission received: 19 February 2019 / Revised: 31 March 2019 / Accepted: 2 April 2019 / Published: 8 April 2019
(This article belongs to the Section Natural Hazards)
Browse Figures
Versions Notes

Abstract

:
The assessment of rockfall risks on human activities and infrastructure is of great importance. Rock falls pose a significant risk to (a) transportation infrastructure, (b) inhabited areas, and (c) Cultural Heritage sites. The paper presents a method to assess rockfall susceptibility at national scale in Greece, using a simple rating approach and Geographic Information Systems (GIS) techniques. An extensive inventory of rockfalls for the entire country was compiled for the period between 1935 and 2019. The rockfall events that were recorded are those which have mainly occurred as distinct rockfall episodes in natural slopes and have impacted human activities, such as roads, inhabited areas, and archaeological sites. Through a detailed analysis of the recorded data, it was possible to define the factors which determine the occurrence of rockfalls. Based on this analysis, the susceptibility zoning against rockfalls at the national scale was prepared, using a simple rating approach and GIS techniques. The rockfall susceptibility zoning takes into account the following parameters: (a) the slope gradient, (b) the lithology, (c) the annual rainfall intensity, (d) the earthquake intensity, and (e) the active fault presence. Emphasis was given on the study of the earthquake effect as a triggering mechanism of rockfalls. Finally, the temporal and spatial frequency of the recorded events and the impact of rockfalls on infrastructure assets and human activities in Greece were evaluated.

1. Introduction

The assessment of rockfall risks on human activities and infrastructure is of great importance. Rock falls pose a significant risk to (a) transportation infrastructure, (b) inhabited areas, and (c) Cultural Heritage sites. The main triggering factors are rainfall, earthquakes, and thermal expansion and contraction. Geological assessment leads to accurate prediction of the outbreak of such events, explains its mechanism of occurrence, and assists in the effective design of protection measures.
In the last decade, Geographic Information Systems (GIS) were used for creating spatial models of potential hazard zonation maps for civil engineering and protection purposes by Mason and Rosenbaum (2002), Mancini et al. (2010), and Calvello et al. (2013) [1,2,3]. Several authors have presented the important role of GIS in hazard assessment and mitigation; these include Carrara et al. (1991), Barredo et al. (2000), Fernandez et al. (2003), Kolat et al. (2006), Yilmaz and Yildirim (2006), Nandi and Shakoor (2009), Paulin et al. (2014) [4,5,6,7,8,9,10], and others.
Susceptibility is the likelihood that an event will occur in a specific area based on the local terrain conditions (Brabb, 1984) [11]. The susceptibility describes the predisposition of an area to be affected by a given future event and results in an estimate of where rockfalls are likely to occur (Guzzetti 2006) [12]. According to Ferrari et al. (2016) [13], susceptibility can be assessed by: (a) geomorphological mapping, (b) empirical and semi-empirical rating systems, (c) statistical analyses, and (d) deterministic methods. The resulting susceptibility maps illustrate the predisposition towards instability of a slope or area. According to Fell et al. (2008) [14], rockfall susceptibility may be assessed based on either a qualitative or quantitative approach. The qualitative approach is based on either field geomorphologic analysis or the combination/overlying of index maps with or without weighting. In the present study, a semi-empirical rating was performed using overlaying of index maps without weighting.
Chau et al. (2003) and Chau et al. (2004) [15,16] presented a rockfall susceptibility map based on a rockfall inventory for Hong Kong using GIS-based techniques at the national level. Carman et al. [17] (2011) prepared a similar map for Slovenia. Trigila et al. (2013) [18] have presented landslide susceptibility mapping at the national scale in Italy using the Italian landslide inventory. Günther et al. (2013) [19] have presented landslide susceptibility assessment for Europe. In Greece, Koukis et al. (2005) and Sabatakakis et al. (2013) [20,21] proposed a landslide hazard zonation and a landslide susceptibility zonation using a landslide inventory derived from historical archives. Antoniou & Lekkas (2010) [22] prepared a rockfall susceptibility map for Santorini Island in Greece using GIS methods. From the pertinent literature review, it is evident that there is no rockfall susceptibility zonation available in Greece.
The geological structure of Greece (frequent occurrence of rock formations, existence of faults and intense fracturing of rockmasses), the steep topography, and its high seismicity, contribute to the outbreak of rockfalls. During the last decades, rockfalls in Greece have become a frequent phenomenon due to intense rainfall events, earthquakes, and the extension of human activities in mountainous areas. Earthquake-triggered rockfalls were specifically investigated in the present study since historical and recent earthquakes in Greece have triggered a significant number of rockfalls, as reported by Papazachos & Papazachou (1997), Pavlides & Caputo (2004), Ambraseys & Jackson (1990), and Saroglou (2013) [23,24,25,26]. More recently, Papathanassiou et al. (2013) [27] investigated the earthquake-induced instabilities in Lefkada Island and Zygouri & Koukouvelas (2015) [28] have studied the evolution of rockfalls triggered by earthquakes in northern Peloponnese. Saroglou et al. (2017) [29] studied the coseismic rockfalls during Lefkada (2015) and Cephallonia (2014) earthquakes and Saroglou et al. (2018) [30] back-analyzed a coseismic rockfall trajectory of the Lefkada 2015 earthquake using UAV-based mapping.
The paper presents an extensive inventory of rockfalls for the period between 1935 and 2019 with events which have mainly occurred in natural slopes and have impacted human activities, such as roads, inhabited areas, and archaeological sites. Rockfalls that have occurred in man-made slopes were not taken into account in the present inventory. The paper also presents a method to assess rockfall susceptibility of natural slopes at national scale in Greece, using a simple rating approach and GIS techniques. The susceptibility map was based on simple rating of specific factors: (a) slope gradient, (b) lithology, (c) rainfall intensity, (d) earthquake intensity, and (e) active fault presence. These factors were selected based on the analysis and evaluation of the rockfall data recorded in the inventory of main rockfall events in Greece between 1935 and 2019. The importance of each factor in relation to the occurrence of rockfalls was investigated.
In the next sections, the rockfall inventory is first presented followed by the susceptibility assessment using GIS. The spatial distribution of rockfall events is evaluated in comparison to the susceptibility map.

2. Rockfall Inventory

A rockfall inventory was created for Greece for the period between 1935 and 2019. Sixty (60) rockfalls events were recorded in forty-three (43) sites, as presented in the national map of Greece shown in Figure 1.
The rockfall events that were recorded are those which have mainly occurred as distinct rockfall episodes in natural slopes and have impacted human activities, such as roads, inhabited areas, and archaeological sites. Rockfalls, which have occurred in man-made slopes (mainly along highways), were not taken into account in the present inventory.
The following data were recorded for each rockfall episode: (a) Location, (b) Coordinates, altitude, (c) Type of site (roadway, inhabited area, archaeological site), (d) Date (s) of rockfall event(s), (d) Triggering mechanism (rainfall, earthquake, other), (e) Fault presence (slope scarp), (f) Geological formation, (g) Rock mass type, degree of fracturing, (h) Slope height, (i) Slope angle, (j) Block size of fallen blocks, (k) Impact (type of affected site), (l) Presence of vegetation (forest etc.), (m) Energy level.
The main recorded parameters of these events are given in Table 1. More details for this rockfall inventory and sources of records were reported in Saroglou (2013) [26].
In some sites, more than one event has occurred and thus it is possible to predict the return period of rockfalls in these cases.
Koukis & Ziourkas (1991) [31] and Koukis et al. (2005) [20] presented a landside frequency zonation map for Greece. The relative frequency of rockfalls, expressed in cases per surface area, was 11%. The maximum frequency of landslides is along the Pindos geotectonic zone, where a large number of slope instabilities occur in the flysch formation in the form of soil type or composite failures (rotational, translational etc.). Based on the present study, the maximum frequency of rockfalls is encountered in western and central Greece.
Rockfalls are generally more frequent in mountainous areas in Greece, where the slope angle is greater than 50 degrees. This is evidenced by the higher occurrence of events in mountainous areas of Greece, such as Pindos and Parnassos Mountain (Figure 1). Rockfalls also occur in low to medium altitude areas where slopes with steep morphology exist, usually related to fault scarps, such as the case of Kakia Scala (Table 1, site 26), Klokova (site 21), and Monemvasia promontory (site 19).

3. Evaluation of the Rockfall Inventory

3.1. Geological Framework and Rockfalls in Greece

The most frequent geological formation encountered in the study areas is limestone (frequency of occurrence equal to 64%). The occurrence of the rocks forming the slopes, as recorded in the database, is presented in Figure 2a. The most frequent geological formation encountered in the rockfall study areas is limestone (with a frequency equal to 64%), while in fewer sites, marble (7%), marls/sandstones (7%), schists/gneisses (3%), and igneous rocks (8%) are encountered.
Generally, limestones are found broken to heavily broken, especially when in the vicinity of faults, resulting in blocky rock masses. Rockfalls are favored in blocky or very blocky rock masses, since medium to large rock blocks are formed by intersecting discontinuities and can be relatively easily detached by the action of water or seismic loading.
In a large number of sites, scree is present at the foot of the slopes. The presence of a scree slope at the base of the rock cliff suggests slope raveling activity. According to Sartori et al. (2003) [32], this activity can be linked to the progressive failure of the rock cliff, but can also be a precursory event of larger rockfalls. Marquínez et al. (2003) [33] presented a rockfall activity index defined as the ratio At/Ar, which correlates with the ability of a certain lithology to produce rockfalls. The index is the ratio of the cartographic surface of the recent talus scree (At) to that of the rocky slope acting as source area (Ar). Dorren & Seijmonsbergen (2003) [34] assigned rockfall susceptibility categories to geological formations according to their nature and ability to produce rocks blocks. They considered limestone to have high susceptibility, while schists, slates, marls, and sandstones low to medium. The block size of the fallen blocks ranges between 0.5 and 50 m3 with an exception of Eptachori rockslide. The blocks size is less than 1 m3 in 22 sites and between 1 and 5 m3 in eight sites, as presented in Figure 2b.

3.1.1. Temporal–Spatial Frequency of Rockfalls

Based on the recorded data, it was possible to define the frequency of rockfalls for the considered time period. The average frequency is one event every 1.3 years, considering the total number of events, irrespective of the rockfall magnitude. For rockfalls with volume of blocks less than 2.5 m3 the return period is 2.8 years, while for events with volume greater than 10 m3, the return period is 16 years. The frequency of rockfalls is shown in Figure 3. It is noted that the number of rockfalls has increased in the 2000–2010 and 2010–2020 decades, which may be attributed to reasons related with climate change (more extreme weather events) or increase of knowledge of rockfall outbreaks through improvement of communication systems.

3.1.2. Triggering Mechanisms

According to the evaluation of the recorded data, the main triggering mechanism of rockfalls is rainfall. Thirteen (13) rockfall events were triggered by rainfall (frequency equal to 33%) and one (1) event by a snowfall. An increase in the number of rockfalls, triggered due to rainfall, has occurred during the last decade mainly due to the occurrence of extreme weather events during the winter periods. This is evidenced, by the occurrence of eighty-six (86) instability phenomena (5% of these were rockfalls) in 2010 (Nikolaou et al., 2011) [35], 95% of which were triggered by intense rainfall during February and the November–December period.
The second most important triggering mechanism was seismic loading as twelve (12) rockfall events were triggered during earthquakes (frequency equal to 25%).

3.1.3. Coseismic Rockfalls in Greece

Earthquakes, which triggered large rockfall events, are those during Alkyonides (1981) and Kalamata (1986) earthquakes, in Skyros Island (2001), in Achaia (2008), in Cephallonia Island (2014), and in Lefkada Island (2003 and 2015). During some of these earthquakes, such as the ones in Kalamata and Achaia, rockfalls occurred along reactivated fault scarps.
The most significant coseismic rockfalls in Greece since 1980 are presented in Table 2, where the location, the date, the magnitude (Mw) of the earthquake, and the distance of the rockfall site from the earthquake epicenter are reported.
The effect of earthquakes on the occurrence of rockfalls is twofold: (a) the magnitude and epicenter distance of an earthquake define whether an unstable block will be detached from a rock slope and (b) the peak ground velocity exerted by an earthquake determines the displacement magnitude of a rock block. Hazard assessment methodologies against earthquake-triggered rockfalls have been applied by Gorum et al. (2011) [36] for the Wenchuan earthquake-induced landslides, by Wasowski & Del Gaudio (2000) [37] in Italy, by Rodriguez-Peces et al. (2011) [38] in Spain, and Marzorati et al. (2002) [39], who produced a rockfall susceptibility map triggered by earthquakes in the Umbria and Marche region in Italy.
Keefer (1984) and Rodriguez et al. (1999) [40,41] developed a magnitude–source distance diagram for landslides, which can also be applied to rockfalls. This diagram (Keefer, 1984) [40] is presented in Figure 4, in which the main coseismic rockfalls from Greece are plotted. The dashed curve presents the maximum distances from fault rupture zones at which disrupted slides and falls have been observed worldwide. Magnitude–distance relations for earthquake-induced landslides in Greece have been proposed by Papadopoulos & Plessa (2000) [42]. More recently, Chousianitis et al. (2016) [43] performed an assessment of the earthquake-induced landslide hazard in Greece, investigating the areal intensity and spatial distribution of slope resistance demand.
The triggering of rockfalls for the events whose epicentral distances plot above the threshold curve is unlikely.
It is obvious that all the coseismic rockfall events in Greece plot well below the curve suggested by Keefer (1984) [40]. The magnitude of earthquakes that triggered rockfalls is between Mw = 5.7 and 6.7, while the maximum distance from the epicenter to a reported rockfall was 36.8 km.

3.1.4. Impact of Rockfalls in Greece

Based on the analysis of the data, the main impact of rockfalls is damage and temporary closure of roadways (frequency equal to 32%) and secondly, damage to houses (frequency equal to 20%). The percentage of potential damage to roadways and houses is 5% and 13%, respectively. The potential damage is defined when a rockfall event poses a direct impact to houses or roadway, but has not impacted them already. Additionally, the percentage of loss of human life is 11%, which is considered exceptionally high. Furthermore, the frequency of potential impact on visitors and damage to archaeological sites is equal to 11%.
The most known and studied events, which have occurred along highways and other roads, are those of Tempi highway (shown in Figure 5b), Kakia Skala (site 26), and Klokova area (site 21). Significant rockfall events impacting roads have taken place in Ag. Nikitas in Lefkada island during the earthquakes in 2003 and 2015 (Figure 5b).
Recent events that affected inhabited areas are those in Eptachori in 1994 (site 17), in Skyros in 2001 (Marinos & Tsiambaos, 2002) [44], Santomeri in 2008 (Koukouvelas et al., 2015 [45]), and Tithorea in 2010 (Saroglou et al., 2015) [46], Plomari in 2018 and Alyki village in 2019. Finally, a house was impacted by a rockfall during a Mw 6.4 earthquake in Lefkada in 2015, resulting in one casualty (Saroglou et al., 2018 [30]).
Sites of high risk in inhabited areas need to be identified in order to minimize rockfall risk. Additionally, there are a large number of rockfall incidents, which have occurred in archaeological sites. These pose a significant danger to tourists and visitors and affect the integrity of the monuments. Such an example is the archaeological site of Delphi (Christaras & Vouvalidis, 2010) [47], where part of the archeological site was closed in 2009. Other affected cultural heritage sites are Mythimna castle (Marinos et al., 2002) [48] and Monemvasia castle (Saroglou et al., 2012) [49], as indicated in Figure 5d.

4. Rockfall Susceptibility

4.1. Introduction

In order to develop the rockfall susceptibility map, GIS techniques in combination with a simple rating approach were used. The main assessment factors were selected based on the evaluation of the recorded data presented earlier. These factors are the following: (1) slope gradient (2) lithology, (3) annual rainfall intensity, (4) earthquake intensity, and (5) active fault presence.
The proximity of a fault has been taken into account only as a qualitative parameter, since it relates to the formation of steep rock cliffs and increased degree of fracturing of rockmass, thus it can be connected to the susceptibility of a rock slope to rockfalls.
Based on these factors, thematic maps for each factor were generated. The rating approach for each factor is described in the following paragraphs.

4.2. Susceptibility Factors

4.2.1. Slope Gradient

Rock slope instabilities occur in steep slopes. The adopted cut off value for slope gradient, above which rock slope instability may occur, is 45°, by analogy with other approaches that give higher values to steeper slopes (Gupta et al., 1999; Meisina et al., 2001) [50,51].
Based on the inventory, the slope angle in the areas with rockfall events ranged between 45 and 90 degrees, while the average slope angle was 70 degrees.
In the present study, a value of 27 degrees was selected. If a value of 45° were to be chosen, the potential rockfall prone areas would be very limited due to the small scale of the map used (1:500.000). The Digital Elevation Model (DEM) was provided by the Hellenic Military Geographical Service (HMGS) in the form of a 25-m density grid of elevation points. A DEM with a spatial resolution of 25 m was created in ARCGIS. The standard ArcView processing was used (Ballifard et al., 2003) [52], which is considered as more appropriate for rough surfaces. The rating for slope gradient is 1 for slopes with angle greater than 27° and 0 for slope angle less than 27°. The slope map is presented in Figure 6.

4.2.2. Lithology

Lithology is a significant factor of the occurrence of rockfalls, since it controls the overall behavior of the geological formation, the degree of fracturing; the permeability of the rockmass and in some occasions the steepness and height of the slope. Rockfalls are favored in blocky or very blocky rock masses, since medium to large rock blocks are formed by intersecting discontinuities and can be relatively easily detached by the action of water or seismic loading.
Dorren & Seijmonsbergen (2003) [34] proposed a rockfall susceptibility of geological formations and assigned rockfall susceptibility categories to them according to their nature and ability to produce rock blocks. They considered that limestone has high susceptibility to generating rockfalls, while schists, slates, marls, and sandstones low to medium. Coe & Harp (2007) [53] presented the influence of tectonic folding on rockfall susceptibility, suggesting that the presence of folds in limestone rocks increases the number of rockfall events. Fityus et al. (2013) [54] performed a detailed study on the significance of geological environment (mainly lithology and tectonic setting) on the morphology and size of potentially unstable blocks.
In the present study, the basic data used to generate the original geological map in vector format were obtained from the existing geological map of Greece published by the Institute of Geology and Mineral Exploration (scale 1:500.000). The main geological formations were grouped into eleven (11) categories based on their lithology, origin, and engineering geological behavior (Figure 7). These were rated with reference to their rockfall susceptibility, thus their ability to produce abundance of rock blocks based on the usual rockmass structure conditions and behavior encountered in these categories. The rating was also based on the evaluation of the rockfall inventory, presented earlier. The susceptibility rating of lithology is presented in Table 3.
The lithology classification map is presented in Figure 8.

4.2.3. Rainfall Intensity

It has been established by many studies that rainfall intensity correlates well with the occurrence of rockfalls. Krautblatter & Moser (2009) [55] proposed a nonlinear model coupling between rainfall and rockfall based on a 4-year monitoring in the Alps. In a number of studies, it is suggested that the maximum precipitation in a 24 h period for a particular return period (50 or 100 years) tends to correlate better with triggering of slope instability phenomena. This is based on the fact that high but regular rainfall tends not to saturate slopes, while lower but irregular rainfall does. Since the assessment is at a national scale, the annual precipitation was chosen for the correlation with rockfall events. A simple rating was proposed considering that rockfall susceptibility increases with annual rainfall intensity. The rating of rainfall intensity is shown in Table 4. The annual precipitation map (Isohyetal contouring) was prepared at an original scale 1:500.000 (Institute of Geology and Mineral Exploration–IGME) and is presented in Figure 9.

4.2.4. Earthquake Intensity

Harp & Jibson (2002) [56] proposed that concentrated seismically triggered rockfalls may result from local amplification of seismic shaking. In order to take into account the effect of earthquakes on the susceptibility, the rating of the acceleration coefficient was considered. Based on the fact that Greece is characterized by three categories with different acceleration coefficients (EPPO, 2003) [57], a simple rating was proposed for earthquake intensity. This rating is summarized in Table 5 and the classification map is presented in Figure 10.

4.2.5. Presence of Faults

Fault zones increase rockfall potential by creating steep slopes and weakened, highly fractured rockmasses. The concept of a fault damage zone has been documented by many authors and a general classification has been published by Kim et al. (2004) [58]. Shipton and Cowie (2003) [59] observed that the damage zone width is approximately 2.5 times the throw, but added that this value is lithology dependent. Brideau et al. (2005) [60] observed that the block size and shape vary as a function of the distance from a fault. The extent of the damage zones that they observed is up to 10 m.
The major faults and thrusts included in the Greek territory have been digitized from the geological map (IGME, scale 1:500.000) and superimposed to form a vector layer. On this layer, a distance function was applied in order to define buffer zones along the structural discontinuities, while two buffer zones, each 250 m wide, were created. The basis of this selection was considering that the estimated width of influence by the presence of a fault in terms of increased fracturing of a rockmass is 250 m. In order to account for the fault presence in the rockfall susceptibility rating, a value of 1 is attributed when a fault is present within a distance of 250 m from the rock slope and a value of 0 is attributed when no fault is present.
Based on the inventory, twenty (20) slopes are related to fault presence and this result in higher rockfall activity. Rondoyanni et al. (2013) [61] has highlighted the importance of presence of active faults on highway slopes in Greece.

4.3. Susceptibility Map

The matrix-based approach is described by a simple index, denoted as Rockfall Susceptibility Index (RSI), which is the sum of the class rating of the aforementioned factors according to the following equation:
RSI = ∑ Lr + Rr + Er + Fr
where: RSI—Rockfall susceptibility index; Lr—lithology; Rr—rainfall intensity; Er—earthquake intensity; Fr—fault presence
Thus, a regional area is more susceptible to rockfalls when the index has lower values. The slope gradient is not summed in the index RSI and when its value is 0, no rockfall occurs. Rockfall susceptibility is classified in three categories, “low” (8 ≤ RSI ≤ 9), “moderate” (5 ≤ RSI ≤ 7), and “high” (3 ≤ RSI ≤ 4), according to a matrix-based approach for all the possible combinations between the categories of the main factors. The rating matrix is presented in Table 6. It is highlighted, that each factor has an equal weight in the calculation of the total susceptibility index.
The spatial distribution of rockfall susceptibility in Greece, based on this approach, is presented in Figure 11. It forms a basis for spatial prediction of the rockfall triggering areas and it gives a general overview of susceptible areas at a national scale. The results of this approach cannot be accurate if the susceptibility is examined at a local scale, since the resolution of the map is quite low for such purposes. Furthermore, it gives guidance for further and more detailed research studies.

5. Discussion

In order to check the reliability of the susceptibility zoning map, the data set of the rockfall inventory presented earlier was used. The susceptibility map accompanied by the locations of the rockfall inventory is shown in Figure 12.
It is evident that the majority of the recorded events are encountered in areas characterized as moderately to highly susceptible to rockfalls. Some events (locations no. 1, 8, 20, 23, and 37) are encountered in areas with low susceptibility. This is anticipated, as the resolution of the susceptibility map is relatively low and thus cannot accurately predict the occurrence of a rockfalls at a regional or local scale. For example, the slope gradient in a small area may be very high due to the presence of a steep rock slope (such as in location no. 1), which is not reflected in the DTM used for the preparation of the susceptibility map.

6. Conclusions

According to the results of the present research, a rockfall susceptibility zoning map for Greece was prepared based on a simple Rockfall Susceptibility Index (RSI). This index is based on the rating of the (a) slope gradient, (b) slope lithology, (c) rainfall intensity, (d) earthquake intensity, and (e) fault presence. The map forms a basis for spatial prediction of rockfall-prone areas at a national scale, while it provides guidance for further and more detailed investigation at the regional scale. It also represents areas exposed to rockfalls and provides the first necessary information towards land use decisions by governmental administrations. Another benefit is that it can assist in the detection of human infrastructure located in susceptible areas which require further analysis, such as hazard and risk.
The reliability of the susceptibility zoning map was checked using a data set of sixty (60) rockfall events for the period between 1935 and 2019. Validation against an independent dataset could be carried out in the future, when new data from rockfalls will be available. Based on the analysis of the recorded data from this inventory, it was evident that the number of rockfalls has increased in recent years.
It was also evident that the main triggering factor was rainfall (33%), while the second most frequent triggering mechanism was earthquake loading (25%). Emphasis was given to investigate the possible presence of faults in rockfall-prone areas and it was shown that half of the rockfall events occurred in slopes were fault scarps exist.
The effect of earthquakes as a triggering mechanism; in particular, the relation with epicenter distance and magnitude of earthquake was also studied. It was found that coseismic rockfall events in Greece were triggered by earthquakes of magnitude between Mw = 5.7 and 6.7, while the distance from the epicenter to a reported rockfall was between 3 and 37 km.
The impact of rockfalls was severe in most cases, mainly resulting in damage to roads and houses (32% and 20% of the total events respectively), while few events resulted in casualties. The potential risk to archaeological sites is also quite high (11% of the total events).
The present study was the first comprehensive study on the occurrence of rockfalls in Greece. It provides a susceptibility zoning assessment at a national scale based on the most important factors, which can prove a valuable decision support tool against rockfall hazards.

Acknowledgments

The author would like to thank I.G.M.E. for providing data from technical reports on rock slope instabilities and I. Kalogeras, National Observatory of Athens for providing data on the studied earthquakes in Greece. The assistance of E. Lykoudi in the preparation of GIS maps is gratefully acknowledged.

Conflicts of Interest

The authors declare no conflict of interest.

References

  1. Mason, P.J.; Rosenbaum, M.S. Geohazard mapping for predicting landslides: An example from the Langhe Hills in Piemonte, NW Italy. Q. J. Eng. Geol. Hydrogeol. 2002, 35, 317–326. [Google Scholar] [CrossRef]
  2. Mancini, F.; Ce-ppi, C.; Ritrovato, G. GIS and statistical analysis for landslide susceptibility mapping in the Daunia area, Italy. Nat. Hazard Earth Syst. Sci. 2010, 10, 1851–1864. [Google Scholar] [CrossRef] [Green Version]
  3. Calvello, M.; Cascini, L.; Mastroianni, S. Landslide zoning over large areas from a sample inventory by means of scale-dependent terrain units. Geomorphology 2013, 182, 33–48. [Google Scholar] [CrossRef]
  4. Carrara, A.; Cardinalli, M.; Detti, R.; Guzzetti, F.; Pasqui, V.; Reichenbach, P. GIS Techniques and statistical models in evaluating landslide hazards. Earth Surf. Process Landf. 1991, 16, 427–445. [Google Scholar] [CrossRef]
  5. Barredo, J.J.; Benavides, A.; Hervas, J.; Van Western, C.J. Comparing heurisitc landslide hazard assessment techniques using GIS in the Trijana basin, Gran Canaria Island, Spain. Int. J. Appl. Earth Obs. Geoinf. 2000, 2, 9–23. [Google Scholar] [CrossRef]
  6. Fernandez, T.; Irigaray, C.; Hamdouni, R.E.; Chacon, J. Methodology for landslide susceptibility mapping by means of a GIS, application to the Contraviesa Area (Granada, Spain). Nat. Hazards 2003, 30, 297–308. [Google Scholar] [CrossRef]
  7. Kolat, C.; Doyuran, V.; Ayday, C.; Suzen, M.L. Preparation of a geotechnical microzonation model using GIS Systems based on Multicriteria decision Analysis. Eng. Geol. 2006, 87, 241–255. [Google Scholar] [CrossRef]
  8. Yilmaz, I.; Yildirim, M. Structural and geomorphological aspects of the Kat landslides (Tokat-Turkey) and susceptibility mapping by means of GIS. Environ. Geol. 2006, 50, 461–472. [Google Scholar] [CrossRef]
  9. Nandi, A.; Shakoor, A. A GIS-based landslide susceptibility evaluation using bivariate and multivariate statistical analyses. Eng. Geol. 2009, 110, 11–20. [Google Scholar] [CrossRef]
  10. Paulin, G.L.; Bursik, M.; Hubp, J.L.; Mejia, L.M.P.; Quesada, F.A. A GIS method for landslide inventory and susceptibility mapping in the Rio El Estado watershed, Pico de Orizaba volcano, Mexico. Nat. Hazards 2014, 71, 229–241. [Google Scholar] [CrossRef]
  11. Brabb, E.E. Innovative approaches to landslide hazard mapping. In Proceedings of the 4th International Symposium on Landslides, Toronto, ON, Canada, 16–21 September 1984; Volume 1, pp. 307–324. [Google Scholar]
  12. Guzzetti, F.; Reichenbach, P.; Ardizzone, F.; Cardinali, M.; Galli, M. Estimating the quality of landslide susceptibility models. Geomorphology 2006, 81, 166–184. [Google Scholar] [CrossRef]
  13. Ferrari, F.; Giacomini, A.; Thoeni, K. Qualitative rockfall hazard assessment: A comprehensive review of current practices. Rock Mech. Rock Eng. 2016, 49, 2865–2922. [Google Scholar] [CrossRef]
  14. Fell, R.; Corominas, J.; Bonnard, C.; Cascini, L.; Leroi, E.; Savage, W.Z. Guidelines for landslide susceptibility, hazard and risk-zoning for land use planning. Eng. Geol. 2008, 102, 85–98. [Google Scholar] [CrossRef]
  15. Chau, K.T.; Wong, R.H.C.; Liu, J.; Lee, C.F. Rockfall hazard analysis for Hong Kong based on rockfall inventory. Rock Mech. Rock Eng. 2003, 36, 383–408. [Google Scholar] [CrossRef]
  16. Chau, K.T.; Tang, Y.F.; Wong, R.H.C. GIS based rockfall hazard map for Hong Kong. Int. J. Rock Mech. Min. Sci. 2004, 41, 846–851. [Google Scholar] [CrossRef]
  17. Čarman, M.; Kumelj, S.; Komac, M.; Ribicic, M. Rockfall susceptibility map of Slovenia. In Proceedings of the Interdisciplinary Rockfall Workshop, Innsbruck, Austria, 16–19 May 2011. [Google Scholar]
  18. Trigila, A.; Frattini, P.; Casagli, N.; Catani, F.; Crosta, G.; Esposito, C.; Iadanza, C.; Lagomarsino, D.; Mugnozza, G.S.; Segoni, S.; et al. Landslide susceptibility mapping at national scale: The Italian case study. In Landslide Science and Practice; Springer: Berlin/Heidelberg, Germany, 2013; pp. 287–295. [Google Scholar]
  19. Günther, A.; Reichenbach, P.; Malet, J.P.; Van Den Eeckhaut, M.; Hervás, J.; Dashwood, C.; Guzzetti, F. Tier-based approaches for landslide susceptibility assessment in Europe. Landslides 2013, 10, 529–546. [Google Scholar] [CrossRef]
  20. Koukis, G.; Sabatakakis, N.; Nikolaou, N.; Loupasakis, C. Landslide Hazard Zonation in Greece; Sassa, K., Fukuoka, H., Wang, F., Wang, C., Eds.; Springer: Berlin/Heidelberg, Germany, 2005; pp. 291–296. [Google Scholar]
  21. Sabatakakis, N.; Koukis, G.; Vassiliades, E.; Lainas, S. Landslide susceptibility zonation in Greece. Nat. Hazards 2013, 65, 523–543. [Google Scholar] [CrossRef]
  22. Antoniou, A.A.; Lekkas, E. Rockfall susceptibility map for Athinios port, Santorini island, Greece. Geomorphology 2010, 118, 152–166. [Google Scholar] [CrossRef]
  23. Papazachos, B.C.; Papazachou, C. The Earthquakes of Greece; Editions ZITI: Thessaloniki, Greece, 1997; 304p. [Google Scholar]
  24. Pavlides, S.; Caputo, R. Tectonophysics Magnitude versus fault’s surface parameters: Quantitative relationships from the Aegean Region. Tectonophysics 2004, 380, 159–188. [Google Scholar] [CrossRef]
  25. Ambraseys, N.N.; Jackson, J.A. Seismicity and associated strain of central Greece between 1890 and 1988. Geophys. J. Int. 1990, 101, 663–708. [Google Scholar] [CrossRef] [Green Version]
  26. Saroglou, H. Rockfall hazard in Greece. Bull. Geol. Soc. Greece 2013, 47, 1429–1438. [Google Scholar] [CrossRef]
  27. Papathanassiou, G.; Valkaniotis, S.; Ganas, A.; Pavlides, S. GIS-based statistical analysis of the spatial distribution of earthquake–induced landslides in the island of Lefkada, Ionian Islands, Greece. Landslides 2013, 10, 771–783. [Google Scholar] [CrossRef]
  28. Zygouri, V.; Koukouvelas, I.K. Evolution of rock falls in the Northern part of the Peloponnese, Greece. IOP Conf. Ser. Earth Environ. 2015, 26, 012043. [Google Scholar] [CrossRef] [Green Version]
  29. Saroglou, H.; Asteriou, P.; Tsiambaos, G.; Manousakis, J.; Zekkos, D. Study of co-seismic rockfalls during Lefkada and Cephallonia Earthquakes, Greece. In Proceedings of the 3rd North American Symposium on Landslides, Roanoke, VA, USA, 4–8 June 2017; pp. 521–528. [Google Scholar]
  30. Saroglou, H.; Asteriou, P.; Zekkos, D.; Tsiambaos, G.; Clark, M.; Manousakis, J. UAV-based mapping, back analysis and trajectory modeling of a coseismic rockfall. Nat. Hazards Earth Syst. Sci. 2018, 18, 321–333. [Google Scholar] [CrossRef]
  31. Koukis, G.; Ziourkas, C. Slope instability phenomena in Greece: A statistical analysis. Bull. Int. Assoc. Eng. Geol. 1991, 43, 47–60. [Google Scholar] [CrossRef]
  32. Sartori, M.; Baillifard, F.; Jaboyedoff, M.; Rouiller, J.-D. Kinematics of the 1991 Randa rockslides (Valais, Switzerland). Nat. Hazards Earth Syst. Sci. 2003, 3, 423–433. [Google Scholar] [CrossRef] [Green Version]
  33. Marquínez, J.; Menéndezduarte, R.; Farias, P.; Jiménez Sánchez, M. Predictive GIS-based model of rockfall activity in mountain Cliffs. Nat. Hazards 2003, 30, 341–360. [Google Scholar] [CrossRef]
  34. Dorren, L.; Seijmonsbergen, A. Comparison of three GIS-based models for predicting rockfall runout zones at a regional scale. Geomorphology 2003, 56, 49–64. [Google Scholar] [CrossRef]
  35. Nikolaou, N.; Pogiatzi, E.; Spanos, N. Report on Landslides in Greece on 2010; I.G.M.E. (Instituto Geologico y Minero de Espana): Madrid, Spain, 2011; p. 8. [Google Scholar]
  36. Gorum, T.; Fan, X.; van Westen, C.J.; Huang, R.Q.; Xu, Q.; Tang, C.; Wang, G. Distribution pattern of earthquake-induced landslides triggered by the 12 May 2008 Wenchuan earthquake. Geomorphology 2011, 133, 152–167. [Google Scholar] [CrossRef]
  37. Wasowski, J.; Del Gaudio, V. Evaluating seismically induced mass movement hazard in Caramanico Terme (Italy). Eng. Geol. 2000, 58, 291–311. [Google Scholar] [CrossRef]
  38. Rodriguez-Peces, M.J.; Garcia-Mayordomo, J.; Azanon, J.; Jabaloy, A. Regional Hazard Assessment of Earthquake-Triggered Slope Instabilities considering Site Effects and Seismic Scenarios in Lorca Basin (Spain). Environ. Eng. Geosci. 2011, 17, 183–196. [Google Scholar] [CrossRef]
  39. Marzorati, S.; Luzi, L.; De Amicis, M. Rock falls induced by earthquakes: A statistical approach. Soil Dyn. Earthq. Eng. 2002, 22, 565–577. [Google Scholar] [CrossRef]
  40. Keefer, D.K. Landslides caused by earthquakes. Bull. Geol. Soc. Am. 1984, 95, 406–421. [Google Scholar] [CrossRef]
  41. Rodriguez, C.E.; Bommer, J.J.; Chandler, R.J. Earthquake induced landslides: 1980–1997. Soil Dyn. Earthq. Eng. 1999, 18, 325–346. [Google Scholar] [CrossRef]
  42. Papadopoulos, G.A.; Plessa, A. Magnitude–distance relations for earthquake–induced landslides in Greece. Eng. Geol. 2000, 58, 377–386. [Google Scholar] [CrossRef]
  43. Chousianitis, K.; Del Gaudio, V.; Sabatakakis, N.; Kavoura, K.; Drakatos, G.; Bathrellos, G.D.; Skilodimou, H.D. Assessment of Earthquake-Induced Landslide Hazard in Greece: From Arias Intensity to Spatial Distribution of Slope Resistance Demand. Bull. Seismol. Soc. Am. 2016, 106, 174–188. [Google Scholar] [CrossRef]
  44. Marinos, P.; Kavvadas, M.; Tsiambaos, G.; Saroglou, H. Rock slope stabilization in Mythimna castle, Lesvos island, Greece. In Proceedings of the 1st European Conference on Landslides, Prague, Czech Republic, 24–26 June 2002; pp. 635–639. [Google Scholar]
  45. Koukouvelas, I.; Litoseliti, A.; Nikolakopoulos, K.; Zygouri, V. Earthquake triggered rock falls and their role in the development of a rock slope: The case of Skolis Mountain, Greece. Eng. Geol. 2015, 191, 71–85. [Google Scholar] [CrossRef]
  46. Saroglou, H.; Berger, F.; Bourrier, F.; Asteriou, P.; Tsiambaos, G.; Tsagkas, D. Effect of forest presence on rockfall trajectory. An example from Greece. In Proceedings of the 12th International Congress of IAEG, Torino, Italy, 13–19 September 2015. [Google Scholar]
  47. Christaras, B.; Vouvalidis, K. Rockfalls in the archaeological site of Delphi, Greece. In Proceedings of the IAEG 2010 International Congress, Auckland, New Zealand, 5–10 September 2010. [Google Scholar]
  48. Marinos, P.; Tsiambaos, G. Earthquake triggering rock falls affecting historic monuments and a traditional settlement in Skyros Island, Greece. In Proceedings of the International Symposium: Landslide Risk Mitigation and Protection of Cultural and Natural Heritage, Kyoto, Japan, 21–25 January 2002; pp. 343–346. [Google Scholar]
  49. Saroglou, H.; Marinos, V.; Marinos, P.; Tsiambaos, G. Rockfall hazard and risk assessment: An example from a high promontory at the historical site of Monemvasia, Greece. Nat. Hazards Earth Syst. Sci. 2012, 12, 1823–1836. [Google Scholar] [CrossRef]
  50. Gupta, R.P.; Saha, A.K.; Arora, M.K.; Kumar, A. Landslide Hazard Zonation in part of the Bhagirathi Valley, Garhwal Mimalyas, using integrated remote sensing—GIS. Himal. Geol. 1999, 20, 71–85. [Google Scholar]
  51. Meisina, C.; Piccio, A.; Tocchio, A. Some aspects of the landslide susceptibility in the Sorba Valley (western Alps, Italy). In Proceedings of the International Conference on Landslides—Causes, Impacts and Countermeasures, Davos, Switzerland, 17–21 June 2001; Kuhne, M., Einstein, H.H., Krauter, E., Klapperich, H., Pottler, R., Eds.; VGE: Essen, Germany, 2001; pp. 547–556. [Google Scholar]
  52. Baillifard, F.; Jaboyedoff, M.; Sartori, M. Rockfall hazard mapping along a mountainous road in Switzerland using a GIS-based parameter rating approach. Nat. Hazards Earth Syst. Sci. 2003, 3, 431–438. [Google Scholar] [CrossRef]
  53. Coe, J.A.; Harp, E.L. Influence of tectonic folding on rockfall susceptibility, American Fork Canyon, Utah, USA. Nat. Hazards Earth Syst. Sci. 2007, 7, 1–14. [Google Scholar] [CrossRef] [Green Version]
  54. Fityus, S.G.; Giacomini, A.; Buzzi, O. The significance of geology for the morphology of potentially unstable rocks. Eng. Geol. 2013, 162, 43–52. [Google Scholar] [CrossRef]
  55. Krautblatter, M.; Moser, M. A nonlinear model coupling rockfall and rainfall intensity based on a four year measurement in a high Alpine rock wall (Reintal, German Alps). Nat. Hazards Earth Syst. Sci. 2009, 9, 1425–1432. [Google Scholar] [CrossRef]
  56. Harp, E.L.; Jibson, R.W. Anomalous concentrations of seismically triggered rock falls in Pacoima Canyon: Are they caused by highly susceptible slopes or local amplification of seismic shaking. Bull. Seismol. Soc. Am. 2002, 92, 180–189. [Google Scholar] [CrossRef]
  57. EPPO. Greek Seismic Code; Earthquake Planning and Protection Organization: Athens, Greece, 2003. [Google Scholar]
  58. Kim, Y.-S.; Peacock, D.C.; Sanderson, D.J. Fault damage zones. J. Struct. Geol. 2004, 26, 503–517. [Google Scholar] [CrossRef]
  59. Shipton, Z.K.; Cowie, P.A. A conceptual model for the origin of fault damage zone structures in high-porosity sandstone. J. Struct. Geol. 2003, 25, 333–344. [Google Scholar] [CrossRef]
  60. Brideau, M.A.; Stead, D.; Kinakin, D.; Fecova, K. Influence of tectonic structures on the Hope Slide, British Columbia, Canada. Eng. Geol. 2005, 80, 242–259. [Google Scholar] [CrossRef]
  61. Rondoyanni, T.; Lykoudi, E.; Triantafyllou, A.; Papadimitriou, M.; Foteinos, I. Active faults affecting linear engineering projects: Examples from Greece. Geotech. Geol. Eng. 2013, 31, 1151–1170. [Google Scholar] [CrossRef]
Geosciences 09 00163 g001 550
Figure 1. Inventory of recorded rockfall events in Greece.
Figure 1. Inventory of recorded rockfall events in Greece.
Geosciences 09 00163 g001
Geosciences 09 00163 g002 550
Figure 2. (a) Lithology in areas of rockfall events, (b) Frequency of block size of fallen rocks.
Figure 2. (a) Lithology in areas of rockfall events, (b) Frequency of block size of fallen rocks.
Geosciences 09 00163 g002
Geosciences 09 00163 g003 550
Figure 3. Frequency of rockfalls for the period between 1935 and 2019.
Figure 3. Frequency of rockfalls for the period between 1935 and 2019.
Geosciences 09 00163 g003
Geosciences 09 00163 g004 550
Figure 4. Magnitude–source distance diagram of coseismic rockfalls in Greece.
Figure 4. Magnitude–source distance diagram of coseismic rockfalls in Greece.
Geosciences 09 00163 g004
Geosciences 09 00163 g005a 550Geosciences 09 00163 g005b 550
Figure 5. Impact of main rockfall events: (a) on local road network in Lefkada during 2003 earthquake (site 3) (b) on National Highway in Tempi valley in 2009 (site 11), (c) in Alyki village in 2019 (site 43), (d) in Monemvasia archaeological site (site 19).
Figure 5. Impact of main rockfall events: (a) on local road network in Lefkada during 2003 earthquake (site 3) (b) on National Highway in Tempi valley in 2009 (site 11), (c) in Alyki village in 2019 (site 43), (d) in Monemvasia archaeological site (site 19).
Geosciences 09 00163 g005aGeosciences 09 00163 g005b
Geosciences 09 00163 g006 550
Figure 6. Slope map of Greece.
Figure 6. Slope map of Greece.
Geosciences 09 00163 g006
Geosciences 09 00163 g007 550
Figure 7. Main geological units encountered in Greece.
Figure 7. Main geological units encountered in Greece.
Geosciences 09 00163 g007
Geosciences 09 00163 g008 550
Figure 8. Thematic map of classification of lithology in Greece.
Figure 8. Thematic map of classification of lithology in Greece.
Geosciences 09 00163 g008
Geosciences 09 00163 g009 550
Figure 9. Thematic map of classification of rainfall intensity in Greece.
Figure 9. Thematic map of classification of rainfall intensity in Greece.
Geosciences 09 00163 g009
Geosciences 09 00163 g010 550
Figure 10. Thematic map of classification of earthquake intensity in Greece.
Figure 10. Thematic map of classification of earthquake intensity in Greece.
Geosciences 09 00163 g010
Geosciences 09 00163 g011 550
Figure 11. Rockfall susceptibility map of Greece.
Figure 11. Rockfall susceptibility map of Greece.
Geosciences 09 00163 g011
Geosciences 09 00163 g012 550
Figure 12. Rockfall susceptibility map and inventory of rockfalls in Greece.
Figure 12. Rockfall susceptibility map and inventory of rockfalls in Greece.
Geosciences 09 00163 g012
Table
Table 1. Main data of recorded rockfalls in Greece.
Table 1. Main data of recorded rockfalls in Greece.
IdLocationTypeDateTriggerRock TypeFault ScarpBlock (m3)Impact
1Santomeri, AchaiaD8/6/2008E (6.5)LY4DH
2Leonidio, TirosR6/1/2008ELY<1RC
3Drimonas, LefkadaD/R14/8/2003E (6.4)LY<1DR
4Lefkada, Ag.NikitasD/R14/8/2003
19/11/2015		E (6.4)
Ε (6.5)		LY13.7
2		PDR
HLL
5Skyros IslandA26/7/2001E (5.8)LY1–2DC
6Ladas, Eleochori, Poliani, KalamataD13/9/1986E (6.2)L <1PDH
7Heraklion (Pitsidia, Akoumia)D14/5/1959E (6.3)LY<1DH
8Geraneia Mt. 24/2/1981E (6.3)LY
9Itea, MonastirakiR18/1/2010E (5.1)LY<1DR
10Konitsa, IoaninnaD/A8/1998ELA 2DH
11Tempi ValleyR17/12/2009
2004,1977 1		NDM 0.5–5, 50HLL, RC
12Kourtaliotis gorgeR4/3/2012RLY1DR
13Pramanta -IoanninaR9/3/2004NDLY<1DR
14AcronafpliaA1/2010NDL 0.5V
15Tithorea, ParnassosD19/12/2010
1999, 1957		NDL 10DH
16Oksilithos, KymiR13/8/2008NDMS 1.5HI
17Eptachori, KastoriaD1935, 51,
68, 70,87, 93, 94		RMY336 2DH
18Delfi ancient siteA2003, 09 1RL 8V
19MonemvasiaA2003, 2010 1RLY2DH, V
20Anc. OlympiaR22/1/2013RL 0.5DR
21Klokova Mt.R16/11/2012NDL 1–2DR
22Therma IkariaD10/1978NDMY1PDH
23Ag. Fotia, CreteR-NDS <1DR
24Taxiarches, LesvosD1963, 3/11/09NDMY1DH
25Mythimna, LesvosA2001RA 0.3ND
26Kakia ScalaR20/11/2000RLY0.5HLL
27Argos CastleA1987NDL D
28Kefalari, ArgosD20/4/2012NDLY0.1HLL
29Stypsi, LesvosD1963, 1977RA 0.5-3.0DH
30Orliagas, ZiakasD/R NDLY1ND
31Carpathos, AkropoliD-NDL -
32Vageni DistomoD/R NDCY40PDR
33KalymnosD12/2002RL 4PDH
34Molaoi, LakoniaD2/2003RCA 1–2PDH
35Chora, IosD-NDS 1PDH
36Vouliagmeni, AtticaD1/1982NDLY1–2
37Kamena VourlaD27/8/2012NDL 1DH
38Nea Pefki, TrikalaR20/10/2010RS <1DR
39Topolia, ChaniaR23/2/2012RLY0.5FB
40SantoriniD2011RP 0.5HLL
41Myrtos, Cephallonia IslandO17/1/2014E (6.1)LY50DR
42Lesvos, PlomariD24/11/2018RSG 10DH
43Alyki, VoiotiaD27/1/2019RL 70DH
1 More rockfall events exist, which are not presented here, 2 the largest rock block, 15 smaller rocks have fallen in this site, Type: R = Roadway, D = Domestic, A: Archeological, O = other (touristic area, coast), Trigger: R = rainfall, E = Earthquake, ND = Not defined, Rock type: L = limestone, M = marble, CA = Calcitic agglomerate, LA = Limestone agglomerate, C = conglomerates, S = sandstone, M = marls, MS = marls/sandstones, SG = Schist/gneiss, A = Andesite, P = Pyroclastics, Fault Scarp: Y = yes, Impact: HLL = Human loss, HI = Human injury, V = Potential impact on visitors, damage to archaeological site, DH = Damage to houses, PDH = Potential house damage, RC = Roadway closure, DR=Damage on roadway, PDR = Potential roadway damage, FB = fall on moving bus, DC = Damage on cars, ND = No damage.
Table
Table 2. Main coseismic rockfalls in Greece.
Table 2. Main coseismic rockfalls in Greece.
No.LocationDateMagnitude (Mw)Rockfall SiteDistance (km)
1Gerania, Korinthos13/9/19866.7Alkyonides27
2Kalamata8/19986Kalamata-Sparti road6.5
3Konitsa14/8/20035.7Eptachori36.8
4Skyros24/2/19816.5Skyros castle20.5
5Lefkada26/7/20016.3Ag. Nikitas7
6Achaia8/6/20086.4Santomeri5.9
7Cephallonia26/01/20145.9Myrtos16.4
8Lefkada11/20156.4Ag. Petros2.8
Table
Table 3. Rating of lithology.
Table 3. Rating of lithology.
Geological FormationRockfall SusceptibilityClass
Postalpine (Marls, claystones, etc.)Low3
GypsumLow3
SchistsLow3
Molasse depositsModerate2
FlyschModerate2
Igneous rocks (granites etc.)Moderate2
Marble–Schist (alternations)Moderate2
DolomitesHigh1
LimestoneHigh1
Volcanic sedimentary rocksHigh1
Gneiss–MarblesHigh1
Table
Table 4. Rating of annual rainfall intensity.
Table 4. Rating of annual rainfall intensity.
Rainfall Intensity (Height of Rainfall per Year)Rockfall SusceptibilityClass
<600 mmLow3
600 mm < R < 1200 mmModerate2
>1200 mmHigh1
Table
Table 5. Rating of earthquake intensity.
Table 5. Rating of earthquake intensity.
Earthquake IntensityRockfall SusceptibilityClass
<0.12 gLow3
0.12 g < a < 0.24 gModerate2
>0.24 gHigh1
Table
Table 6. Rating matrix for the calculation of Rockfall Susceptibility Index (RSI). Category of low susceptibility in grey, moderate in green, and high in red.
Table 6. Rating matrix for the calculation of Rockfall Susceptibility Index (RSI). Category of low susceptibility in grey, moderate in green, and high in red.
RSIEarthquake (class 1)Earthquake (class 2)Earthquake (class 3)
Lithology + Rainfall classes (sum = 2) 345
Lithology + Rainfall classes (sum = 3)456
Lithology + Rainfall classes (sum = 4)567
Lithology + Rainfall classes (sum = 5)678
Lithology + Rainfall classes (sum = 6)789

Share and Cite

MDPI and ACS Style

Saroglou, C. GIS-Based Rockfall Susceptibility Zoning in Greece. Geosciences 2019, 9, 163. https://doi.org/10.3390/geosciences9040163

AMA Style

Saroglou C. GIS-Based Rockfall Susceptibility Zoning in Greece. Geosciences. 2019; 9(4):163. https://doi.org/10.3390/geosciences9040163

Chicago/Turabian Style

Saroglou, Charalampos. 2019. "GIS-Based Rockfall Susceptibility Zoning in Greece" Geosciences 9, no. 4: 163. https://doi.org/10.3390/geosciences9040163

APA Style

Saroglou, C. (2019). GIS-Based Rockfall Susceptibility Zoning in Greece. Geosciences, 9(4), 163. https://doi.org/10.3390/geosciences9040163

Note that from the first issue of 2016, this journal uses article numbers instead of page numbers. See further details here.

Article Metrics

Back to TopTop