The Environmental Seismic Intensity Scale (ESI 2007) in Greece, addition of new events and its relationship with magnitude in Greece and the Mediterranean; preliminary attenuation relationships

Quaternary International xxx (2017) 1e19

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The Environmental Seismic Intensity Scale (ESI 2007) in Greece, addition of new events and its relationship with magnitude in Greece and the Mediterranean; preliminary attenuation relationships Ioannis Papanikolaou a, *, Maria Melaki a, b a Laboratory of Mineralogy & Geology, Department of Natural Resources Development and Agricultural Engineering, Agricultural University of Athens, 75 Iera Odos Str., 11855 Athens, Greece b Laboratory of Natural Hazards, Faculty of Geology and Geoenvironment, National and Kapodistrian University of Athens, Panepistimiopolis 157 84, Athens, Greece

a r t i c l e i n f o

a b s t r a c t

Article history: Received 8 April 2016 Received in revised form 21 May 2017 Accepted 24 May 2017 Available online xxx

The Environmental Seismic Intensity (ESI) scale has been officially released in 2007 and is based on the quantification of Earthquake Environmental Effects. Due to its quantitative nature, the scale improves the process of assessing macroseismic intensities, particularly in the epicentral area of those cases in which sole traditional intensity scales prove to be ineffective. Following a large number of publications that applied this relatively newly established scale, there is some need for parametrization. This is because this intensity scale can offer new insights to seismic hazard assessment and has the potential to reduce the uncertainties that stem from traditional macroseismic scales. This study has three main goals. Firstly, to enrich and compile an ESI 2007 database from earthquakes in Greece by adding 4 new events. Secondly, to extract a relationship between Magnitude and the ESI 2007 for Greece and the Mediterranean. Thirdly, to offer a preliminary estimate of how the intensity attenuates with distance, after developing a code in Python language to assist this process. The ESI 2007 scale was applied in the 1995 Ms ¼ 6.6 Kozani-Grevena earthquake, the 1978 Mw ¼ 6.5 Thessaloniki earthquake, the historic 1894 Atalanti earthquake sequence (M ¼ 6.4 and M ¼ 6.8) and the 365AD event in Crete (M ¼ 8.4). These events were selected because they have well documented and extensive co-seismic effects, including primary and secondary surface ruptures, rockfalls, landslides and liquefaction phenomena. For the Kozani earthquake, extracted results were correlated with SAR interferograms, in order to provide a complete and high spatial resolution of the ground deformation. Both the Kozani-Grevena and the Thessaloniki events produced a maximum intensity IX on the ESI 2007 scale, the Atalanti earthquake produced a maximum intensity X and the 365AD Crete earthquake a maximum intensity XII. Overall, the ESI 2007 scale compares fairly well with the traditional macroseismic scales except for some villages in the KozaniGrevena epicentral area where due to the poor quality of buildings, existing scales overestimated the intensity by one degree compared to the ESI 2007. It is interesting to note that both for Greece and the Mediterranean area a strong correlation exists between Mw and the ESI 2007 scale. In particular, the following relationships between the Mw and the ESI scale have been extracted: i) for Greece Io(ESI 2007) ¼ 3.1427 exp (0.1643Mw) and ii) for the Mediterranean Io(ESI 2007) ¼ 3.3543exp (0.1557Mw). However, more events and more data regarding the intensity distributions are required to establish the intensity attenuation with distance. © 2017 Elsevier Ltd and INQUA. All rights reserved.

Keywords: Kozani-Grevena earthquake Atalanti earthquake sequence Thessaloniki earthquake Earthquake Environmental Effects ESI 2007 scale Attenuation laws

1. Introduction

* Corresponding author. E-mail addresses: [email protected] (I. Papanikolaou), [email protected], [email protected] (M. Melaki).

The Environmental Seismic Intensity (ESI 2007) scale, introduced by INQUA (International Union for Quaternary Research), is a twelve-degree structured scale, which takes into account solely the Earthquake Environmental Effects (EEE), both primary and

http://dx.doi.org/10.1016/j.quaint.2017.05.044 1040-6182/© 2017 Elsevier Ltd and INQUA. All rights reserved.

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secondary ones, caused by a seismic event (Michetti et al., 2007). In particular, it considers the occurrence, size and areal distribution of EEE, including surface faulting, tectonic uplift and subsidence, landslides, rock falls, liquefaction, ground collapse, hydrological effects and tsunami waves (Michetti et al., 2004, 2007). The ESI 2007 provides a quantitative analysis and description of the EEE, thus offering a further effective tool for assessing macroseismic intensities. Its use provide an added value because unlikely other traditional scales EEE are not influenced by human parameters, such as manmade structures (Guerrieri et al., 2007). When damage in manmade structures is used to assess the macroseismic intensity (as traditional scales do), intensity will tend to reflect mainly the economic development and the cultural setting of the area that experienced the earthquake, instead of its “strength” (Serva, 1994). The latter introduces a large uncertainty in the intensity assignment and attenuation relationships. The use of many different intensity scales worldwide (e.g. MM, MS, MCS, MSK64, JMA), which are also constantly updated (e.g. EMS 1992, EMS 1998, etc.) in order to incorporate new types of buildings or design features, indirectly demonstrates the deficiency of such earthquake intensity scales in describing the earthquake macroseismic effects (Papanikolaou, 2011). As a result, the ESI 2007 has been developed, forming a simple tool to calibrate earthquake size in a straightforward and quantitative mannerbased on environmental effects (Michetti et al., 2004; Serva et al., 2016). The ESI 2007 is not designed to replace the previous scales, that record the macroseismic effects in the engineering environment, but complement them by offering as a calibrating factor the geoenvironment. Effects in the natural environment were initially included in some previous macroseismic scales, (e.g. MSK64), but they did not differentiate between primary and secondary effects nor they were following any quantitative approach. As a result, through time the environmental parameters have been neglected and sidelined. Among other advantages, this scale: (i) allows the comparison among future, recent and historical earthquakes as well as events from different tectonic settings (e.g. Michetti et al., 2004; Porfido €chert, 2009; et al., 2007; Serva et al., 2007; Buchner and Kro Guerrieri et al., 2009; Papathanassiou et al., in press), (ii) allows the assessment of the seismic intensity in sparsely populated or inhabited areas (Tatevossian, 2007; Mosquera-Machado et al., 2009; Comerci et al., 2015a; Serva et al., 2016) and (iii) allows the intensity evaluation, where traditional scales saturate (i.e. for intensities X to XII) and only the coseismic environmental effects can be considered as diagnostics (Michetti et al., 2004; Lekkas, 2010; Sanchez and Maldonado, 2016), (iv) can offer high spatial resolution (e.g. Ota et al., 2009; Silva et al., 2013) since EEE can vary significantly over short distances and more importantly can manifest everywhere since they are not constrained by the presence of manmade structures, thus increasing the sample, v) can support seismic hazard assessment by inferring intensity values of pre-instrumental earthquakes from paleoseismological data (e.g. Serva et al., 2016) and reducing the large uncertainties introduced from existing attenuation relationships by offering objective criteria in drawing the isoseismals (Papanikolaou, 2011), vi) even when surface ruptures are not positively recognized in historical documents or confirmed from fieldwork data, the total area affected by secondary environmental effects can yield a quite accurate assessment of epicentral intensity as has been demonstrated in several events (e.g. 1805 Molise, Porfido et al., 2002, Serva et al., 2016; the 1887 Verny, Tatevossian, 2007). The ESI 2007 scale was developed in the framework of INQUA, thus in early publications it was referred as the INQUA-EEE scale (e.g. Papathanassiou and Pavlides, 2007; Guerrieri et al., 2007; etc). The idea of a new intensity scale based on the environmental effects was initially introduced in 1999, during the 15th INQUA

Congress in Durban, South Africa. In the frame of INQUA SubCommission in Paleoseismicity, a Working Group including geologists, seismologists and engineers coordinated by the Geological Survey of Italy compiled a first version of the scale, that was presented at the 16th INQUA Congress in 2003 in Reno, USA and was updated one year later at the 32nd International Geological Congress in Florence, Italy (Michetti et al., 2004). The INQUA TERPRO (Commission on Terrestrial Processes) approved a specific project (INQUA Scale Project, 2004e2007) with the aim of: a) testing the scale for a trial period of 4 years, b) reviewing the first version through its application to case studies worldwide, and c) submitting the revised version, so as to be ratified during the 17th INQUA Congress in Cairns (Michetti et al., 2007). Then, during the 17th INQUA Congress, the use of the ESI 2007 scale was officially approved. Since 2007 several projects developed within the framework of the INQUA TERPRO Focus Group on Paleoseismology lead to the compilation of EEE catalogues, whereas the last INQUA Project 1229P focused also on the parameterization of Earthquake Environmental Effects and the development of relationships between source parameters and the ESI 2007 intensity. The current publication follows this path. As a result, the ESI 2007 scale has now been applied in a plethora of events in Greece and worldwide with tens of publications and has been translated in 10 languages (Audemard et al., 2015; ISPRA). In addition, the concept of the ESI scale has been successfully transferred to Archaeoseismology and tsunami hazards with the establishment of the Earthquake Archeological Effects (EAE) (Rodríguez-Pascua et al., 2011) and the Integrated Tsunami Intensity Scale (ITIS-2012) (Lekkas et al., 2013). The ESI 2007 incorporates the recent advances of Earthquake Geology and Paleoseismology and is now regarded as a major tool for fault specific seismic hazard assessment (Reicherter et al., 2009; Papanikolaou et al., 2015) and it can be useful for insurers, civil protection agencies and planners (Serva et al., 2016). Indeed, Papanikolaou (2011) demonstrated that the attenuation relationships of traditional intensities form a major source of uncertainty in seismic hazard assessment and in several cases they overshadow all the other factors of uncertainty, even fault slip-rates, which govern the earthquake occurrence. Therefore, parametrization of the ESI scale by correlating it with the earthquake magnitude and the development of attenuation relationships can be valuable for seismic hazard assessment. Following the above, the goals of this study are: a) to expand the existing ESI 2007 database for Greece (see Appendix 1), by adding new events with well documented EEE (Sections 2, 3, 4 and 5); b) compile a database for Greece (Section 6.1) and one for the Mediterranean (Section 6.2); c) test if and how the ESI 2007 values correlate with the earthquake magnitude, offering some tables of correlation (Section 7) and d) try to extract and explore some preliminary data regarding the attenuation of the ESI 2007 intensities with distance (Section 6.3). In order to enrich the existing database for Greece, three destructive events have been studied in detail and the maximum ESI 2007 value for the 365AD event has been assessed (Fig. 1). These events are the 1995 Ms ¼ 6.6 KozaniGrevena earthquake (western Macedonia region), the 1978 Mw ¼ 6.5 Thessaloniki (central Macedonia region), and the historic 1894 Atalanti earthquake sequence (M ¼ 6.4 and M ¼ 6.8) (Central Greece). 2. The May 13, 1995, Kozani-Grevena earthquake An Ms ¼ 6.6 (Mw ¼ 6.5) earthquake occurred on May 13, 1995 in north-central Greece (western Macedonia region, Fig. 1). The epicentre was at a depth of approximately 10 km (Papazachos et al., 1998). The earthquake activated a ENE-WSW trending normal

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Fig. 1. The epicentres of the 15 seismic events from Greece. With green events studied in the current study, with red events extracted from the literature. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.)

fault dipping to NNW (Mountrakis et al., 1998). The affected area (Fig. 2) comprised a wide zone trending aprox. E-W, from the northwest boundary of the molassic formation of the “Meso-Hellenic Trench” through the ophiolitic complex of Vourinos Mt and the carbonates of “Almopia”, to the neotectonic basin of Kozani (Papanikolaou, 2015). This event caused severe damages on human infrastructures. More than 15 villages and towns suffered significant damage (Carydis et al., 1995). Hundreds of buildings collapsed, including houses, schools, churches and hospitals. In addition, extensive co-seismic environmental effects were recorded including primary surface ruptures and numerous secondary effects (Fig. 2). 2.1. Primary effects

maximum intensity IX on the ESI 2007 scale. Two main fracture lines, the Rymnio-Paleochori-Sarakina-Nisi line and the ChromioVaris-Mirsina line, associated with the main and the antithetic fault respectively were observed in the field (Pavlides et al., 1995; Mountrakis et al., 1998). The most impressive ruptures were formed along the Paleochori-Sarakina fault that was the main activated structure approximately 15 km long with maximum displacements up to 20 cm and visible rupture length up to 3 km (Mountrakis et al., 1998). The activation of the antithetic Chromio-Mirsina Fault caused ruptures with vertical displacements up to a few tens of cm along a discontinuous line of at least 2 km. Detailed data concerning the ruptures were collected from Mountrakis et al. (1998), Pavlides et al. (1995) and Stamatis (1995) (Fig. 2).

Significant surface ruptures were recorded, implying a Please cite this article in press as: Papanikolaou, I., Melaki, M., The Environmental Seismic Intensity Scale (ESI 2007) in Greece, addition of new events and its relationship with magnitude in Greece and the Mediterranean; preliminary attenuation relationships, Quaternary International (2017), http://dx.doi.org/10.1016/j.quaint.2017.05.044

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Fig. 2. The spatial distribution of the Kozani-Grevena EEE (Mountrakis et al., 1998; Lekkas et al., 1996; Pavlides et al., 1995; Stamatis, 1995) and a simplified geological map. 1: Alluvial and Scree, 2: Plio-Pleistocene sediments (fluvial and lacustrine sediments, mostly marls, loose conglomerates and at places sandstones), 3: “Tsotylion” molassic formation, 4: “Pendalofo” molassic formation, 5: “Vourinos” ophiolitic complex, 6: “Eastern Greece” carbonates, 7: “Flambouron” gneisses and schists (after Lekkas et al., 1996).

2.2. Secondary effects Liquefaction phenomena were observed along an extensive 4 km long and more than 2 km wide zone at the southern shore of the Polyfytos artificial lake, responsible for the >80 cm subsidence of the Eani-Rymnio bridge paving (Pavlides et al., 1995). Ground cracks and cracks on the roads with maximum displacements up to 10 cm were recorded all over the earthquake-stricken area (Pavlides et al., 1995; Mountrakis et al., 1998). Major landslides occurred near the villages of Knidi, Rymnion, Kentron and Kalamitsi and rock falls occurred towards the steep slopes of the Aliakmon river banks (Lekkas et al., 1996). These data were imported and processed into a GIS and EEE (Fig. 2) and intensity maps (Fig. 3) were produced. In addition to ground observations, the existence of SAR data for this event offered a useful tool that provided a detailed and high spatial resolution view of the deformation field (Rigo et al., 2004). As a result, for the assignment and mapping of the ESI 2007 intensity values, field observations were combined with SAR data (Fig. 3a). It is important to note that the lines that bounded the deformation of 28 mm and 280 mm of the interferogram were considered as the boundaries for intensity VIII and IX respectively. Taking into account the effects and the local geological setting, a maximum intensity IX on the ESI 2007 scale was extracted. The estimated affected area of the EEE is about 900 km2, in agreement with the ESI 2007 scale for Intensity IX.

2.3. ESI 2007 and comparison with the damage pattern and traditional macroseismic scales During the shock and the aftershock activity, up to 1000 buildings were collapsed and over 7000 infrastructures suffered severe damage, including 30 school buildings, 2 hospitals and 17 churches (Carydis et al., 1995). Papazachos et al. (1998) assessed the maximum intensity value as IX-X (they actually refer it as IXþ, that according to Papazachos and Papazachou, 1997; equals 9þ ¼ 9.5 so IX-X). This value is more or less in agreement with the maximum intensity IX of the ESI 2007. This area was allocated to the lowest zone I (pga ¼ 0.12 g) of the National Seismic Building Code before the earthquake, because no major historical or instrumental events have been recorded in the area. However, following the earthquake the area was upgraded to a higher zone II (pga ¼ 0.16 g, 10% probability of exceedance in 50 years E.P.P.O.-A.C.E.G., 2001). Geologic data indicate repeated Late PleistoceneeHolocene slip, but with very long recurrence intervals (Chatzipetros et al., 1998). Following the above and the perception of the local population of an aseismic region with no memory of moderate or strong earthquakes, the majority of the buildings in the affected area were built of adobe or non seismic design unreinforced masonry or non-seismic reinforced concrete. Only the most recent buildings were built with reinforced concrete frames and experienced minor damages (Lekkas et al., 1996). These

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Fig. 3. a) Digitized fringes obtained by InSAR data. The numbers correspond to the subsidence range change in mm (Rigo et al., 2004), b) the ESI 2007 isoseismal map based on the InSAR data and EEE.

poor quality buildings tend to sustain very high or up to 100% damages above intensity VIII. For example, adobe is expected to sustain 100% damage for intensity IX, 80% damage for non seismic design unreinforced masonry and 70% damage for reinforced concrete frames of non seismic design (see Table 1; Sauter and Shah,

1978; Degg, 1992). As a result, assessing precisely the maximum epicentral intensity by means of the traditional macroseismic scales was a difficult process due to saturation levels at intensities  VIII. This reflects the inadequacy of the traditional scales for such cases. Furthermore, we tried to evaluate the damage pattern and

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Table 1 Description of the earthquake loss susceptibility data for different construction types (Sauter and Shah, 1978; Degg, 1992). Building Characteristics

Construction Type (x3)

Average damage (%) VII

Adobe Non seismic design unreinforced masonry Reinforced concrete frames non seismic design Reinforced concrete frames seismic design

1 2 3 4

compare it with the ESI 2007 scale after taking into account the percentage of the damage caused to buildings in the affected area. Such data regarding the % of damaged buildings in the epicentral locality were collected from a report composed by Lekkas et al. (1995). These data are superimposed on the geological map and the ESI 2007 isoseismals VIII and IX for comparison (Fig. 4). Villages that suffered the most devastating damage are mainly built on PlioPleistocene fluvial and lacustrine sediments (e.g. Chromio, Kalamitsi, Varis, Kalochio villages founded on alternations of predominantly marls, some loose conglomerates and occasionally sandstones), or at short distances from the primary ruptures (e.g. Paleochori, Sarakina, Kentro), except for the village of Knidi that is founded on the Lower Miocene “Tsotylion” molassic formation, consisting of weathered alternations of conglomerates, sandstones and marls (Lekkas et al., 1995). The poor foundation conditions due to the weakness of the geological formations are also confirmed by the large number of fractures, slides and liquefaction phenomena that extend the ESI 2007 intensity VIII into a relatively large area.

VIII

IX

X

(y1)

(y2)

(y3)

(y4)

22% 14% 11% 4%

50% 40% 33% 13%

100% 80% 70% 33%

100% 100% 100% 58%

The damage pattern demonstrated that the geological setting was the predominant parameter, whereas the topographic effects had little or no influence (Lekkas et al., 1996; Hadjinakos et al., 1998). When comparing the evnironmental effects and the ESI 2007 isoseismals, it is clear that 4 villages that sustained major damages up to devastation, are located within ESI 2007 intensity VIII (Fig. 4). These are the villages of Chromio (94% damage), Kalamitsi (97% damage), Mesolakkos (>80%), and Kalochio (>80%) (Fig. 4). The latter implies that the damage pattern significantly exceeds the relatively low ESI 2007 intensities. The relatively low ESI 2007 maximum intensity IX compared to the damage pattern, confirms the poor quality of the buildings. This is a similar outcome to the 1997 Colfiorito earthquake in Italy whereas the ESI 2007 values were lower than the MCS ones due to the poor quality and poor maintenance of the buildings (Guerrieri et al., 2009).

Fig. 4. Geological map showing the % of damaged villages following the report by Lekkas et al. (1995) and the ESI 2007 isoseismals for intensity VIII and IX. Four villages that sustained severe damages (>80%) are located within VIII isoseismal. This low ESI 2007 intensity value compared to the damage pattern, confirms the poor quality of the buildings.

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3. The April, 1894 Atalanti earthquake sequence The region of Lokris (along the southern coast of the Gulf of Evia) was struck by two pre-instrumental large seismic events that occurred one week apart, on 20th and 27th April 1894 respectively. There are some uncertainties regarding the magnitudes and both epicentres, however, recent reanalyses, estimate the magnitudes as M ¼ 6.4 and M ¼ 6.8 respectively (Pantosti et al., 2001).

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with vertical displacements up to 30 cm in the limestone that exceeded 1 m in alluvium (Skouphos, 1894; Papavassiliou, 1894a,b). Extensive surface faulting occurred, extending from Martino to Atalanti villages, for about 25 km (Ambraseys and Jackson, 1990). The most severe effects were observed towards the coastline, where the shore subsided and the peninsula of Gaidouronisi was transformed into an island, with an estimated elevation change of 30e80 cm during the second shock (Cundy et al., 2000). These effects imply a maximum ESI 2007 intensity X.

3.1. Description of earthquake environmental effects The earthquakes produced extensive damage and significant EEE (Fig. 5). During the first shock, all the villages between Megaplatanos and Martino were devastated and 223 people were killed. The second event extended the damage pattern towards the NW in the villages between Megaplatanos and Agios Konstantinos, an area not affected by the first shock, killing 30 people (Ambraseys and Jackson, 1990). However, it is difficult to separate the damages caused by each shock, because they were closely spaced in time. 3.2. Primary effects Extensive surface ruptures and tectonic subsidence were observed. Several researchers (Skouphos, 1894; Mitsopoulos, 1895; Lemeille, 1977; Ambraseys and Jackson, 1990; Ganas et al., 1997; Pantosti et al., 2001) have described the ruptures caused by these events, still visible today. Initial reports described surface ruptures

3.3. Secondary effects During the first shock, the coastal plain from Almyra to Livanates liquefied. However, liquefaction phenomena during the second event occurred in sites distant up to 40 km from the epicentral area (Ambraseys and Jackson, 1990). This shock triggered major landslides and seismic sea-waves, flooding a wide area between the villages of Agios Konstantinos and Almyra, but the estimates regarding the extension of the inundation vary significantly among authors (Skouphos, 1894; Mitsopoulos, 1895; Cundy et al., 2000). However, the coastal zone between Almyra and Kato Peli, remained flooded (Cundy et al., 2000). In order to create a complete ESI 2007 intensity map (Fig. 6), in spite of the few EEE intensity values available, the latter were correlated with the pattern of deformation produced by Cundy et al. (2000), based on an elastic half-space dislocation model.

Fig. 5. The spatial distribution of the Atalanti Earthquake sequence EEs (Ambraseys and Jackson, 1990; Lemeille, 1977; Pantosti et al., 2001; Ganas et al., 1997; Skouphos, 1894) and a simplified geological map (modified based on Albantakakis, 1978; Katsikatos et al., 1984; Maratos et al., 1965, Maratos et al., 1967; Marinos et al., 1957; Papastamatiou et al., 1971; Tataris et al., 1970). The lines represent the contours of equal deformation of the ground in cm, as estimated from the elastic dislocation model of Cundy et al. (2000).

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Fig. 6. The ESI 2007 isoseismal map of the 1894 Atalanti earthquake sequence. The map was compiled by combining the EEE intensity values with the deformation pattern derived from an elastic dislocation model Cundy et al. (2000).

3.4. ESI 2007 and traditional macroseismic scales According to Skouphos (1894) and NewspaperAcropolis (1894), Malesina, Martino, Proskunas and Mazi were totally destroyed during the first shock (Fig. 7). Extensive damage has also been recorded all over the earthquake stricken area (Atalanti, Proskinas, Livanates, Kiparissi) as well as on Northern Evia, where numerous infrastructures collapsed (Arkitsa, Agia Anna, Limni and the Lichades penisnula). Despite the building damage records in Northern Evia, no earthquake environmental effects have been reported. However, we do not know whether they have occurred but noone has recorded them, or they have not occurred. The latter implies that the geographical distribution of secondary effects can not be well constrained and therefore the ESI 2007 isoseismals VI, VII and VIII can not be accurately mapped. During the second earthquake, the already vulnerable buildings collapsed and damages have been recorded all over the Atalanti, Dadi and Thronio municipalities and the Lichas peninsula (North Evia). Several records exist regarding the damage effects of the two earthquakes (Skouphos, 1894; Papavassiliou, 1894a, 1894b; NewspaperAcropolis, 1894; IllustratedLondonNews, 1894; Mitsopoulos, 1895; Ambraseys and Jackson, 1990; Sieberg, 1932; Papazachos and Papazachou, 1997). Albini and Pantosti (2004) analysed all the records in order to assess and draw EMS98 macroseismic intensities (Fig. 7) for both events. The question marks in Fig. 7b indicate 6 sites (Martino, Malessina, Kiparissi, Proskinas, Tragana, Mazi) that were already destroyed by the first event; therefore, no data regarding the intensity was gathered following

the second event. This example, illustrates the saturation problems that traditional intensities face for high intensity  IX values and emphasize once again the importance of the EEE effects for mapping high intensity values. We have overlapped the ESI local intensities with the EMS98 intensity map (Fig. 7c). Differences are noteworthy, especially regarding the intensity IX isoseismals. This may reflect the poor quality of the buildings in the earthquakestruck area that played a decisive role in the damage distribution.

4. The June 20, 1978 Thessaloniki earthquake A Mw ¼ 6.5 earthquake occurred on June 20, 1978 in northern Greece (central Macedonia region Fig. 1) and specifically in the area between the Koronia lake and the Volvi lake (Roumelioti et al., 2007, Fig. 8). The earthquake nucleated at a depth of approximately 8 km (Carver and Bollinger, 1981). This main shock was the result of an intense seismic activity that initiated on May 23 and two strong earthquakes occurred before the main shock. The first on May 23 (Mb ¼ 5.7; Mercier et al., 1983) and the second one on June, 19 (M ¼ 5.2; Roumelioti et al., 2007). This earthquake attracted a lot of interest, since it was the first strong instrumental event that has occurred near a major urban centre, in particular 25 km NE of Thessaloniki, a city of almost 700.000 inhabitants. Even though modern buildings performed reasonably well during the shock and the damages were not extensive, 45 fatalities, 220 injuries and extensive EEE have been observed near the epicentral area (Papazachos and Papazachou, 1997).

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Fig. 7. The EMS 1998 intensity map of (a) the April 20, 1894 Atalanti event and (b) the April 27, 1894 Atalanti event. Intensity data from Albini and Pantosti (2004). Question marks indicate sites where intensity values could not be evaluated due to saturation effects, (c) Comparison of the isoseismal pattern between the EMS 1998 and the ESI 2007 intensity scales.

4.1. Description of earthquake environmental effects Numerous earthquake environmental effects were observed in the meizoseismal area, including surface ruptures, seismic induced slidings and liquefaction phenomena. The majority of these EEE were observed in the area between the two lakes of Langada and Volvi. This area is susceptible for such effects since it forms a recent tectonic depression covered by Quaternary deposits (Fig. 8). 4.2. Primary effects Extended surface ruptures have been observed and the vast majority of the researchers consider them as primary effects

(Mercier et al., 1983; Papazachos et al., 1979). Analysis of geodetic data suggested that the event was associated with 25 cm of subsidence, expressing doubts on whether the seismic fault reached the surface (Stiros and Drakos, 2000). However, the primary character of the surface ruptures are supported by the relatively high displacement values and the fact that the surface faulting was traced either very close or up to the geological fault traces (e.g. Tranos et al., 2003). Thus, in this study these ruptures were considered as primary. Two main fracture lines were recorded, the Stivos-Scholari line and the Peristeronas-Gerakarou line with vertical displacements up to 25 cm and 23 cm respectively (Papazachos et al., 1979). The visible length of the fracture lines was up to 8 km and 12 km respectively (Papazachos et al., 1979). In

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Fig. 8. The spatial distribution of the Thessaloniki EEE (Mercier et al., 1983; Papazachos et al., 1979; Psycharis, 1978) on a simplified geological map (modified from Mountrakis et al., 1997 1:100.000 neotectonic map).

general, the length of the ruptures was up to 2 times smaller than the fault length deduced from the aftershocks distribution (Soufleris and Stewart, 1981). 4.3. Secondary effects Not all the observed surface breaks were of tectonic origin; some of them had been clearly affected by gravitational sliding (Mercier et al., 1979) and extensive liquefaction phenomena particularly at short distances from the lakes. Craters with diameter up to 3 m and up to 70 cm deep were recorded (Psycharis, 1978). Moreover, en echelon ground cracks were observed parallel to the main fracture lines with visible length ranging from a few tens of meters up to 600m (Mercier et al., 1983; Papazachos et al., 1979). Hydrological changes, such as overflowing wells due to the rise of aquifer level were mentioned (Psycharis, 1978). 4.4. ESI 2007 and traditional macroseismic scales The observed EEE imply a maximum ESI 2007 intensity IX. Subsequently, published field observations were combined with geodetic data (Stiros and Drakos, 2000) and slip distribution models (Roumelioti et al., 2007) in order to produce the ESI 2007 isoseismal map for intensities VIII and IX of the 1978 event (Fig. 9). Extensive damage caused by the earthquake affected both the epicentral area between the lakes as well as the town of Thessaloniki, where an 8-storey building collapsed and 3170 buildings suffered non repairable damage. Overall, 9470 buildings suffered non repairable damage and 23,589 suffered severe damage over 4 prefectures (Thessaloniki, Kilkis, Serres and Chalkidiki) (Papazachos and Papazachou, 1997). However, modern buildings of

that time sustained no or minor damage mostly of masonry failures (Psycharis, 1978). Thus, the majority of the studies were focused on Thessaloniki, and mainly on the recorded damages, the vulnerability of the buildings and on microzonation studies (Penelis et al., 1988; Theodulidis et al., 2006). In the epicentral area, a VIII-IX maximum intensity value of the Modified Mercalli Intensity scale (MMI) was recorded in the villages of Stivos, Gerakarou and Scholari (Papazachos and Papazachou, 1997). These villages are within the intensity IX of the ESI 2007 scale (Fig. 9), so both scales agree well on their spatial distribution, even if the MM scale slightly underestimates the intensity. Recent Quaternary sediments, the steep topography generated by the range bounding active faults and the two lakes contributed to the manifestation of secondary effects such as liquefaction and sliding phenomena. In Thessaloniki, even if the evaluated MS intensity was VI-VII (Papazachos et al., 1997), no enviromental effects were recorded. This is not only due to the distance from the epicentre, but also because the diagnostic effects of the ESI 2007 scale for intensities of VI and below are minor or non-existent. Overall, the ESI 2007 scale may not accurately describe the damage in the far field. Even if no EEE are observed due to the long distance, if the dominant period of the soil is approximately equal to the dominant period of certain buildings, severe damage can occur to them (e.g. up to 70 km away in Athens 1981, Papanikolaou et al., 2009; or even 350 km away in Mexico 1985, Serva et al., 2016). 5. The 365 AD earthquake A mega-earthquake equivalent to an Mw 8.3e8.5 event (Shaw et al., 2008) struck the eastern Mediterranean area on July 21, 365AD which is probably the strongest historical European event.

Please cite this article in press as: Papanikolaou, I., Melaki, M., The Environmental Seismic Intensity Scale (ESI 2007) in Greece, addition of new events and its relationship with magnitude in Greece and the Mediterranean; preliminary attenuation relationships, Quaternary International (2017), http://dx.doi.org/10.1016/j.quaint.2017.05.044

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11

Fig. 9. The ESI 2007 isoseismal map of the 1978, Thessaloniki earthquake. The map was produced by combining the EEE intensity values with geodetic data (Stiros and Drakos, 2000) and slip distribution models (Roumelioti et al., 2007).

According to historical and archeological evidence, the earthquake and the tsunami triggered after the shock destroyed many cities, inundated coastal sites (from Alexandria to the Sicily and Adriatic Sea; Guidoboni et al., 1994; Smedile et al., 2011) and caused thousand of fatalities. This event was directly or indirectly reported by more than 30 ancient authors (Jacques and Bousquet, 1984). Due to this seismic event a massive area has been uplifted from the Antikythira island westwards up to central Crete, whereas the western part of Crete uplifted up to 9 m (Spratt, 1865; Thommeret et al., 1981; Pirazzoli et al., 1996; Stiros, 2001, 2010; Shaw et al., 2008; Stiros, 2010). Shaw et al. (2008) concluded that the 365AD earthquake produced 20e25 m of slip on a ~100 km long fault, dipping northeast at 30 from the Hellenic Trench to a depth of 45 km. Polonia et al. (2016) confirmed based on the study of giant turbidity currents and radiocarbon dating that a single basin-wide event (e.g. the 365AD earthquake), was able to resuspend sediments over a very wide region including the Mediterranean Ridge, the Ionian abyssal plain, the Tyro Basin, and the Sicily and Calabria slopes. In addition, the 365 AD tsunami sediments still preserved today at high elevations of 6e7 m above sea level both in NW Crete (at Phalasarna ancient port (e.g. Pirazzoli et al., 1992; DomineyHowes et al., 1998) and southern Crete (Werner et al., submitted)) also testify for this major event. The 9 m vertical crust uplift, is the predominant evidence so as to assess the maximum ESI 2007 intensity XII for this event. In addition, the estimated 20e25 m of slip on the fault and the evidence of high-energy waves deposits several meters above the present sea level along the coastal sites of southwestern Crete offer additional support for the maximum ESI 2007 XII.

6. ESI 2007 attenuation relationships In order to define the seismic hazard at a given site, it is necessary to know the maximum expected intensity and its attenuation with distance from the epicenter. The ESI 2007 scale may prove beneficial for the seismic hazard assessment by reducing the present day large uncertainty implied in the attenuation laws. In order to achieve this, first it is important to establish a relationship between the magnitude and the ESI 2007 scale and then calculate how the intensity attenuates with distance. 6.1. ESI 2007 dataset for Greece and relationship between earthquake magnitude and the ESI 2007 scale An ESI 2007 database for 15 well documented events in Greece has been compiled. It comprises 11 events extracted from the literature and 4 events described in the previous sections (see Appendix 1) (Fig. 1). Thus, a relationship between earthquake

Table 2 Relationship between Ms and ESI 2007 for Greece. Ms

5.5e6.0 6.1e6.5 6.6e7.0 8.1e8.5

N

5 5 4 1

Magnitude Ms

Intensity (ESI 2007)

min

max

mean

min

max

mean

5.5 6.3 6.6 e

6.0 6.5 6.8 e

5.83 6.40 6.70 8.40

VII-VIII VIII-IX IX e

IX X X e

VIII IX IX-X XII

8.20 9.00 9.63 12.00

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magnitude and the ESI 2007 is offered. Tables 2 and 3 show the relationship between the Ms and Mw with the ESI 2007 in Greece. All the earthquake magnitudes were converted to moment magnitude (Mw), using the relations suggested by Scordilis (2006) (Ms to Mw) and Okal and Talandier (1989) (Mm to Mw). Table 3 shows that earthquakes of Mw ¼ 5.9, Mw ¼ 6.3 and Mw ¼ 6.7 are expected to produce a maximum (Io) ESI 2007 intensity value of VIII, IX, and X, respectively. The correlation between the Mw and the ESI 2007 in Greece is provided by the following relationship: Io(ESI 2007) ¼ f(Mw) Io ¼ 3.1427 exp (0.1643Mw)

6.2. Relationship between magnitude and the ESI 2007 for the Mediterranean In total, 35 well documented earthquakes for which ESI 2007 intensities have been extracted formed a database for the Mediterranean (Appendix 1). These events are from Greece, Italy, Spain, Slovenia and Algeria published by several research groups. Table 4 shows the relationship between Mw and the ESI 2007 for the Mediterranean region. Table 4 shows that earthquakes of Mw ¼ 4.7, Mw ¼ 5.9, Mw ¼ 6.3, Mw ¼ 6.8 and Mw ¼ 7.2 are expected to produce a maximum (Io) ESI 2007 intensity value of VII, VIII-IX, IX, IX-X and X respectively. The correlation between the Mw and the ESI 2007 in the Mediterranean is provided by the following relationship: Io(ESI 2007) ¼ f(Mw) Io ¼ 3.3543exp (0.1557Mw)

6.3. Preliminary attenuation relationships Isoseismals are lines that separate areas characterised by different intensity values and represent the spatial distribution of the macroseismic information obtained by the quantification of the effects and damage produced by an earthquake. The isoseismal maps are used to derive empirical relations for the decrease of intensity with distance, which then are incorporated into the attenuation laws and used to assess the seismic hazard (e.g. Papanikolaou, 2011). Thus, isoseismal lines had to be drawn for each earthquake and then the events from the catalogue having a complete isoseismal pattern have to be evaluated. However, due to incompleteness of data regarding the isoseismal distribution of some intensity degrees (e.g. for older events or coastal areas or island settings), this process was feasible for a limited number of events. Indeed, a credible and complete spatial distribution is available only for 8 events from Greece and Italy regarding intensities IX and VIII (Table 5). All these events correspond to normal faulting earthquakes, therefore they offer a more homogenous sample in terms of the focal mechanism and the seismic source characteristics.

Table 3 Relationship between Mw and ESI 2007 for Greece. Mw

5.6e6.0 6.1e6.5 6.6e7.0 8.1e8.5

N

4 7 3 1

Magnitude Mw

Intensity (ESI 2007)

min

max

mean

min

max

mean

5.7 6.1 6.6 e

6.0 6.5 6.8 e

5.92 6.34 6.70 8.40

VII-VIII VIII-IX IX-X e

VIII-IX X X e

VIII IX X XII

8.00 9.00 9.83 12.00

Table 4 Preliminary table showing the relationship between Mw and ESI 2007 for Mediterranean events. Mw

4.0e5.5 5.6e6.0 6.1e6.5 6.6e7.0 7.1e7.5 8.1e8.5

N

3 8 9 11 3 1

Magnitude Mw

Intensity (ESI 2007)

min

max

mean

min

max

mean

4.2 5.6 6.1 6.6 7.2 e

5.2 6.0 6.5 7.0 7.2 e

4.70 5.89 6.32 6.82 7.20 8.40

VI-VII VII-VIII VIII-IX IX IX e

VIII IX X XI XI e

VII VIII-IX IX IX-X X XII

7.16 8.31 9.00 9.59 10.00 12.00

6.3.1. Algorithm development In order to calculate the intensity attenuation with distance from the macroseismic epicenter, an algorithm in python language has been developed (Appendix 2). The algorithm avoids any subjectivity in the process of calculating the intensities' radius. This algorithm is used for the determination of the macroseismic epicenter and the estimation of the mean radius of the isoseismals IX and VIII. After isoseismals IX and VIII have been drawn and an image has been extracted, the algorithm converts this image in grey scale, based on a RGB model. Subsequently, the macroseismic epicenter is determined as the barycenter of the isoseismal IX line, and after the real coordinates of the image have been inserted, the algorithm defines the coordinates of the epicenter. The algorithm scans the isoseimal IX and all the radius from the epicenter to the isoseismal line are estimated and placed into a table. The same procedure is used for the isoseimal VIII. Finally, the maximum, minimum and mean distances from the epicenter to the isoseismals of intensity VIII and IX are extracted. 6.3.2. Results The results of this process for the 8 normal faulting events are displayed in Table 6. The mean radius of the isoseismals IX and VIII are estimated as 9128 m and 19307 m respectively. However, these need to be grouped based on their epicentral Io. Indeed four events with Io ¼ IX have a mean radius of 6534 m of isoseismal IX and 12657 m of isoseismal VIII, whereas 2 events with Io ¼ X have a mean radius of 10009 m of isoseismal IX and 25666 m of isoseismal VIII and 2 events with Io ¼ ХІ have a mean radius of 12511 m of isoseismal IX and 32795 m of isoseismal VIII. These preliminary results show a relatively smooth decrease of the intensity radius as approaching a lower epicentral І0 and are regarded as reasonable. Even though the sample is clearly small, it provides a first pattern of the intensity attenuation with distance for normal faulting events in the Mediterranean area. 7. Discussion Intensity attenuation relationships are a major tool for seismic hazard assessment and the construction of seismic hazard maps, thus are closely related to the prevention and seismic risk management. Hence, these relationships are important for determining the hazard pattern. The quantitative nature of the ESI 2007 and the sufficient guidelines for the survey of EEEs (Michetti et al., 2007) leave little room for subjectivity, decreasing the uncertainty in assigning intensity values and, in addition, may offer higher spatial resolution than traditional scales that are constrained by the presence of the manmade environment (Papanikolaou, 2011; Serva et al., 2016; Silva et al. in press). The latter is of major importance so as to build complete and credible attenuation relationships between the earthquake magnitude and the intensity scale. As a result, a re-appraisal of historical and recent earthquakes so as to

Please cite this article in press as: Papanikolaou, I., Melaki, M., The Environmental Seismic Intensity Scale (ESI 2007) in Greece, addition of new events and its relationship with magnitude in Greece and the Mediterranean; preliminary attenuation relationships, Quaternary International (2017), http://dx.doi.org/10.1016/j.quaint.2017.05.044

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Table 5 Summary table showing the radius (maximum, minimum, mean) of isoseismals IX and VIII for 8 well constrained normal faulting events from the Mediterranean. Earthquake Characteristics

Intensity VIII

Intensity IX

Region

Year

Mw

Io

Rmin

Rmax

Rmean

Rmin

Rmax

Rmean

Messina Straits Calabria Molise Irpinia-Basilicata Kozani Kalamata Sofades Thessaloniki

1908 1783 1805 1980 1995 1986 1954 1978

7.2 7 7.2 6.9 6.5 6.1 6.8 6.5

XI XI X X IX IX IX IX

12,374 15,426 17,734 7963 6466 5461 8879 4882

76,022 44,012 34,857 39,057 18,785 9367 26,462 23,699

36,833 28,757 26,881 24,451 14,236 6884 16,171 13,338

7370 10,896 4720 4087 4380 1682 5308 3279

16,084 16,509 15,172 14,225 9250 6694 7593 11,864

11,407 13,614 10,266 9751 7605 4720 6365 7446

Table 6 The mean radius of isoseismals IX and VIII for different maximum epicentral intensities Io. Io

Number of events

Mean Magnitude (Mw)

INTENSITY ESI2007 Isoseismal VIII

Isoseismal IX

IX X XI

4 2 2

6.48 7.05 7.10

Rmean ¼ 12,657 m Rmean ¼ 25,666 m Rmean ¼ 32,795 m

Rmean ¼ 6534 m Rmean ¼ 10,009 m Rmean ¼ 12,511 m

constrain the ESI 2007 scale and the extraction of ESI-based attenuation laws may prove beneficial for the seismic hazard assessment by reducing the uncertainty implied in the existing attenuation laws and eventually in the seismic hazard maps (Papanikolaou, 2011). Hazard maps are highly sensitive to the expected intensity at a site and its attenuation with distance from the epicenter. Therefore, the compilation of the ESI 2007 database (Appendix 1) allowed the extraction of a relationship between magnitude

and the maximum expected intensity Io for Greece and for the Mediterranean. Following the above, Fig. 10 was constructed in order to show whether the Mw correlates with the ESI 2007 maximum intensity. It is important to note that both diagrams display a high correlation both for Greece (R2 ¼ 0.76) and the Mediterranean (R2 ¼ 0.72) respectively. In Greece, almost all the events with well documented EEE have been compiled; therefore the dataset is not expected to be significantly differentiated in the future.

Fig. 10. a) Diagram showing the correlation between the Mw and the ESI 2007 scale in Greece. b) Diagram showing the correlation between the Mw and the ESI 2007 scale for the Mediterranean. Both diagrams show a strong correlation between Mw and the ESI 2007 scale.

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As more well documented events bolster the database, the reliability of these relationships will be further enhanced. However, the existing high correlation already reflects a strong trend that it is not expected to be modified significantly. It is also clear that there is a gap for very strong events higher than M > 7.0 in Greece and M > 7.2 for the Mediterranean. This is because the vast majority of earthquakes in the area occur in extensional settings, whereas active normal faults tend to have an upper magnitude threshold of around M ¼ 7.1 to M ¼ 7.2. The results of Fig. 10b are in good agreement with events from other settings such as the 2004 Chuetsu event (Mw ¼ 6.6 and IX ESI 2007, Ota et al., 2009) and the 1995 Kobe event (Mw ¼ 6.9 and X ESI 2007, Ota et al., 2009). In addition, several very strong events ranging from Mw ¼ 7.3 up to Mw ¼ 7.6, with well documented EEE have all maximum ESI 2007 intensity XI. In particular the 1992 Mw ¼ 7.3 Murindo strike slip event (Mosquera-Machado et al., 2009), the 1976 Mw ¼ 7.5 Guatemala strike slip event (Porfido et al., 2015), the 1999 Mw ¼ 7.6 Chi-Chi thrusting event (Ota et al., 2009) and the 2005 Mw ¼ 7.6 Pakistan thrusting event (Ali et al., 2009). Therefore, despite the fact that currently there is gap in the Mediterranean for Mw ¼ 7.3 to Mw ¼ 7.6, these worldwide events confirm the relationship of Fig. 10b, adding more confidence to the existing correlation. Following the above, it would be interesting to trace the lowest earthquake magnitude where the ESI 2007 intensity XII is observed. According to existing published data the lowest threshold has been positively traced around Mw ¼ 7.9 (based on the 2008 Mw ¼ 7.9 Wechuan earthquake (Lekkas, 2010) and the 2002 Mw ¼ 7.9 Denali strike slip event (Comerci et al., 2015a). As a result, even though Fig. 10b has been constructed based on well documented (mostly normal faulting: 25 events) Mediterranean events, the extracted relationship is in agreement also with major worldwide events from different tectonic settings. The accurate assessment of the maximum epicentral intensity (Io) is of major importance. This is because the Io assessment significantly affects not simply the magnitude estimate for historical events, but also the intensity attenuation with distance. Table 6 shows how important is the correct identification of the Io for estimating the attenuation with distance and the generation of seismic hazard maps. A preliminary relationship has been extracted for ESI 2007 intensities IX and VIII from 8 well documented normal faulting events for the Mediterranean, but it is clear that the sample needs to be enlarged. The intensity distribution, however, depends on the availability of observations and for several earthquakes in Greece and the Mediterranean information is often lacking. For example, isoseismals are often constrained either due to the lack of detailed observations for older historical events or due to the sea, since several of the earthquakes occurred in coastal areas or islands, thus not permitting an objective intensity assessment towards the offshore setting. A larger sample should be one of the future emerging goals. In addition, the extraction of similar relationships for other types of earthquakes in thrusting and strike slip environments could also offer a first pattern of the intensities attenuation. The algorithm developed herein in Python language (Appendix 2) may be a useful tool for these purposes. Despite the fact that the ESI 2007 is an additional effective tool that can reduce the uncertainties in the intensity assignment and attenuation laws compared to the traditional scales, some uncertainties will remain. For example, regional seismotectonic features, such as the thickness of the seismogenic layer and/or a characteristic high or low stress-drop may play a role in increasing the uncertainty (e.g. the Baikal region; Tatevossian et al., 2010). For example, stress drop is strongly variable from one setting to another, or even from one fault to another and this might also be

related to time-dependent fault healing, so that the stress drop is simply a function of recurrence intervals (e.g. Nadeau and McEvilly, 1999; Scholz, 2002; Fry et al., 2010). In addition, the flexural strength of the lithosphere could also be major factor that controls primary effects (Scholz and Conteras, 1998). In these settings the sample might not be enough to produce local scaling relationships.

8. Conclusions The ESI 2007 scale has been applied in four earthquake events from Greece with well documented EEE. The 1995 Kozani-Grevena and the 1978 Thessaloniki earthquakes produced a max ESI IX, whereas the 1894 Atalanti event a max ESI X and the 365 AD a max ESI 2007 XII. For the 1978 event the ESI 2007 compares fairly well with the traditional macroseismic scales. In the 1995 Kozani event the maximum ESI 2007 epicentral intensity correlates well with maximum traditional macroseismic intensities, but in several localities the ESI 2007 underestimates the traditional intensities. A similar pattern is also partly evident in the Atalanti event for intensity IX. However, for the epicentral area of the Atalanti events the saturation of the damage to buildings did not allow a complete comparison for intensities  X. This underestimation of intensity IX for both events is attributed to the poor quality of the buildings. SAR interferograms offer a complete and high spatial resolution of the ground deformation and form a useful tool for mapping EEEs for recent events. Similarly dislocation models validated by fieldwork data and reports might be used for older events in order to reconstruct the deformation field. Seismic hazard assessment is highly sensitive to the expected intensity at a site and its attenuation with distance from epicentre. The ESI 2007 scale, offers the opportunity to reduce the involved uncertainties, since its quantitative nature, through the study of Earthquake Environmental Effects and the absence of human parameters, provides further information useful to improve intensity assessment. An ESI 2007 database with well documented events for Greece and the Mediterranean has been compiled. Subsequently, a relationship between the magnitude Mw and the expected ESI 2007 values was established. The high correlation both for the events of Greece and for the earthquakes from the Mediterranean area (R2 ¼ 0.761 and R2 ¼ 0.720 respectively) reflects a stable trend. A preliminary relationship for normal faulting events for intensities IX and VIII provides a first order pattern of how the ESI 2007 intensity attenuates with distance. For this purpose an algorithm in Python Language has been compiled. It is rather unlikely that all uncertainties implied by the attenuation/amplification can be fully reduced, however, as more data from recent and historical events are gathered, the development of accurate ESI 2007 attenuation laws will improve the accuracy of the seismic hazard maps.

Acknowledgements: This contribution forms part of the INQUA projects 1229P Parametrization of Earthquake Environmental Effects and Project 1619R GEMAP - Geological Earthquake Mapping of recent, historical and paleoseismic events: Quaternary Geology for Seismic Hazard Analyses. Alessandro Maria Michetti, Dimitrios Papanikolaou, and Eythimios Lekkas are thanked for discussions regarding the ESI 2007 scale. Comments by both reviewers greatly improved the manuscript.

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Appendix 1. Database with 35 well documented earthquakes with ESI 2007 intensities in the Mediterranean.

Greece

Earthquake

Date

Magnitude Converted magnitude Mw

ESI2007 Fault Type

References

1 2

Lefkada Kephalonia

11/17/2015 01/26 & 02/03/ 2014

6.4 (Mw) 5.9/ 6.0(Mw)

6.4 6.0

VIII-IX VIII

strike-slip strike-slip

Papathanassiou et al., 2016 Lekkas and Mavroulis, 2015

instrumental instrumental

3 4 5 6 7 8 9 10 11

Andravida Lefkada Athens Kozani-Grevena Pyrgos Elia Kalamata Alkyonides Aklyonides

6.4 (Mw) 6.4 (Ms) 5.9 (Ms) 6.6 (Ms) 5.5 (Ms) 5.9 (Ms) 6.0 (Ms) 6.3 (Ms) 6.7/6.4 (Ms) 6.5 (Ms) 6.8 (Ms) 6.4/6.8

6.4 6.2 6.0 6.5 5.7 6.0 6.1 6.3 6.7/6.4

IX VIII-IX VIII-IX IX VII-VIII VIII IX X X

strike-slip strike-slip normal normal normal normal normal normal normal

Papathanassiou et al., in press Mavroulis et al., 2013 Papathanassiou et al., 2007 Fokaefs and Papadopoulos, 2007 This study Papanikolaou et al., 2009 Fokaefs and Papadopoulos, 2007 Fountoulis and Mavroulis, 2013 Papanikolaou et al., 2009 Papanikolaou et al., 2009

instrumental instrumental instrumental instrumental instrumental instrumental instrumental instrumental instrumental

6.5 6.8 6.4/6.8

IX IX-X X

normal normal normal

This study Papathanassiou et al., 2007 This study

15 Crete

01/08/2008 08/14/2003 09/07/1999 05/13/1995 03/26/1993 10/16/1988 09/13/1986 03/04/1981 02/24 & 02/25/ 1981 06/20/1978 04/30/1954 04/20 & 04/27/ 1894 07/21/365

~8.4 (Ms)

~8.4

XII

thrust

16 Amatrice

08/24/2016

6.0 (Mw)

6.0

IX

normal

17 18 19 20 21

Finale Emilia Abruzzo Umbria-Marche Irpinia Irpinia

05/20/2012 04/06/2009 09/26/1997 11/23/1980 07/23/1930

5.9 6.3 6.0 6.9 6.6

(Ml) (Mw) (Mw) (Mw) (Mw)

5.8 6.3 6.0 6.9 6.6

IX IX IX X X

22 23 24 25

Fucino Messina Straits Calabria Bojano

01/13/1915 12/28/1908 09/08/1905 07/26/1805

7.0 (Ms) 7.2 (Me) 7.0 6.9 (Mm)

7.0 7.2 7.0 7.2

X XI XI X

thrust normal normal normala Oblique normalb normal normal normal normal

02/05/1783

7.0 (Mw)

7.0

XI

normalc

12 Thessaloniki 13 Sofades 14 Atalanti

Italy

28 Irpinia-Basilicata 09/05/1694

6.9 (Mm)

7.2

IX

normal

Serva et al., 2007

29 Sannio

06/05/1688

6.7 (Mm)

7.0

VIII

normalf

Serva et al., 2007

30 Lorca 31 Albolote 32 Huercal- Overa

03/11/2011 04/19/1956 06/10/1863

5.2 (Mw) 5.0 (Ms) 4,2 (M)

5.2 5.4 4.2

VII VIII VI-VII

thrustg normalh thrusti

Silva et al., 2014a Silva et al., 2014a Silva et al., 2014a

33 Estubeny

03/23/1748

6,2 (M)

6.2

IX

normalj

Silva et al., 2014a

04/12/1998

5.6 (Mw)

5.6

VII-VIII thrust

Gosar, 2012

instrumental instrumental instrumental preinstrumental preinstrumental preinstrumental preinstrumental preinstrumental instrumental instrumental preinstrumental preinstrumental instrumental

5/21/2003

6.8 (Mw)

6.8

X

Heddar et al., 2016

instrumental

26 Calabria 27 Umbria

Spain

instrumental instrumental preinstrumental This study preinstrumental Livio et al., 2016, Piccardi et al., 2016, Guerrieri instrumental et al., sub Di Manna et al., 2012 instrumental ISPRA instrumental Guerrieri et al., 2009 instrumental Serva et al., 2007 instrumental Serva et al., 2007 instrumental

Slovenia 34 Slovenia (Krn Mount) Algeria 35 Boumerdes

01/14/1703

6.8 (Mw)

6.8

X

Blumetti et al., 2015

d

ISPRA

e

normal

thrust

ISPRA Comerci et al., 2015b ISPRA Serva et al., 2007

Ms: Surface Wave Magnitude, Mm: Mantle Magnitue, Ml: Local Magnitude, Me: Energy Magnitude, Mw: Moment Magnitude. a Del Pezzo et al., 1983. b Pino et al., 2008. c Jacques et al., 2001. d Westaway, 1992. e Chiaruttini and Siro, 1991. f Pantosti and Valensise, 1988. g Morales et al., 2014. h Sanz de Galdeano et al., 2012. i Silva et al., 2014b. j Buforn et al., 2015.

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Appendix 2. The algorithm, in Python language, that has been developed in order to calculate how the intensity attenuates with distance. The program comprises 8 steps. In particular: Step 1 insert the info regarding the library data that will be used. Step 2 activates the path that will read the black and red isoseismal lines and after using the library cv2 transforms them into black (intensity IX) and grey (intensity VIII). Step 3, it calculates the number of pixels based on the length and width of the picture. Step 4 considering the real coordinates (in m) that the user inserts, it calculates the real dimensions of every pixel. Step 5 According to the RGB model, 0 corresponds to full black whereas 255 to full white. The 5th step isolates and selects the pixels where 0 is traced (isoseismal IX) and introduce them into a table that is called perimeter. The barycenter (the

macroseismic epicentre) of pixels is calculated using the mean command form the library nb and names it as “centre”. Step 6 after using the X and Y values extracted from the previous step and knowing the real dimensions of every pixel from the 4th step, the real coordinates of the barycentre are extracted. Step 7 a table is compiled (dists) that is filled up with the distances (in m) of all the points (pnt) of the black line (perimeter) from the barycentre (centre). Step 8 the max, min and mean value of the above distances are extracted that correspond to the max, min and mean radius of the isoseismal IX for every earthquake. Steps 5 to 8 are repeated also for the grey (perimeter2) isoseismal of intensity VIII after using a range of values (70 &  175) corresponding to the grey color. Finally the algorithm constructs and saves a new B&W picture that illustrates both isoseismal lines (black and grey) as well as the barycentre extracted from the previous step.

Please cite this article in press as: Papanikolaou, I., Melaki, M., The Environmental Seismic Intensity Scale (ESI 2007) in Greece, addition of new events and its relationship with magnitude in Greece and the Mediterranean; preliminary attenuation relationships, Quaternary International (2017), http://dx.doi.org/10.1016/j.quaint.2017.05.044

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Please cite this article in press as: Papanikolaou, I., Melaki, M., The Environmental Seismic Intensity Scale (ESI 2007) in Greece, addition of new events and its relationship with magnitude in Greece and the Mediterranean; preliminary attenuation relationships, Quaternary International (2017), http://dx.doi.org/10.1016/j.quaint.2017.05.044