the Creative Commons Attribution 4.0 License.

the Creative Commons Attribution 4.0 License.

# From regional to local SPTHA: efficient computation of probabilistic tsunami inundation maps addressing near-field sources

### Stefano Lorito

### Jacopo Selva

### Roberto Tonini

### Fabrizio Romano

### Beatriz Brizuela

Site-specific seismic probabilistic tsunami hazard analysis (SPTHA) is a computationally demanding task, as it requires, in principle, a huge number of high-resolution numerical simulations for producing probabilistic inundation maps. We implemented an efficient and robust methodology using a filtering procedure to reduce the number of numerical simulations needed while still allowing for a full treatment of aleatory and epistemic uncertainty. Moreover, to avoid biases in tsunami hazard assessment, we developed a strategy to identify and separately treat tsunamis generated by near-field earthquakes. Indeed, the coseismic deformation produced by local earthquakes necessarily affects tsunami intensity, depending on the scenario size, mechanism and position, as coastal uplift or subsidence tends to diminish or increase the tsunami hazard, respectively. Therefore, we proposed two parallel filtering schemes in the far- and the near-field, based on the similarity of offshore tsunamis and hazard curves and on the similarity of the coseismic fields, respectively. This becomes mandatory as offshore tsunami amplitudes can not represent a proxy for the coastal inundation in the case of near-field sources. We applied the method to an illustrative use case at the Milazzo oil refinery (Sicily, Italy). We demonstrate that a blind filtering procedure can not properly account for local sources and would lead to a nonrepresentative selection of important scenarios. For the specific source–target configuration, this results in an overestimation of the tsunami hazard, which turns out to be correlated to dominant coastal uplift. Different settings could produce either the opposite or a mixed behavior along the coastline. However, we show that the effects of the coseismic deformation due to local sources can not be neglected and a suitable correction has to be employed when assessing local-scale SPTHA, irrespective of the specific signs of coastal displacement.

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In the last 15 years a number of large earthquakes occurred worldwide, often accompanied by destructive tsunamis. In several cases, the overall size of the earthquake and/or of the tsunami was unanticipated and some surprising features were observed in terms of event scaling (e.g., source aspect ratio, tsunami height versus earthquake magnitude) or associated damage (Lay, 2015; Lorito et al., 2016); a striking example is the 2011 Tohoku earthquake and tsunami and the consequent nuclear disaster at the Fukushima Daiichi power plant (Synolakis and Kânoğlu, 2015). These events called attention to the need for a systematic reevaluation of current tsunami hazard estimates.

In the past, tsunami hazard was mostly studied through simulations of one or several scenarios, either the “worst credible” (e.g., Tinti and Armigliato, 2003; Lorito et al., 2008; Tonini et al., 2011; Løvholt et al., 2012a) or representative of different selected return periods (e.g., Løvholt et al., 2006; Harbitz et al., 2012; Brizuela et al., 2014; Gailler et al., 2015). Such an approach can be useful either as a first screening of tsunami hazard or to realize very detailed assessments for informing emergency managers of the potential impact of specific scenarios. Traditionally, the latter is often also done as a result of probabilistic hazard disaggregation (Bazzurro and Cornell, 1999).

To account for potential variability and frequency of tsunamis, and for the inclusion of alternative models needed for quantifying epistemic uncertainty, the probabilistic treatment of a large set of potential tsunami sources is essential. Probabilistic tsunami hazard analysis (PTHA) probably began with the seminal papers of Lin and Tung (1982) and Rikitake and Aida (1988). Uncertainty quantification is one of the main goals of PTHA, and progressively more refined uncertainty treatment was achieved following the 2004 Indian Ocean tsunami (e.g., Geist and Parsons, 2006; Burbidge et al., 2008; González et al., 2009; Horspool et al., 2014; Hoechner et al., 2016; Selva et al., 2016; Davies et al., 2017; Grezio et al., 2017; Power et al., 2017). PTHA is becoming the established good practice for managing risk assessment and risk mitigation measures (Chock et al., 2016; Løvholt et al., 2017). Due to the lack of historical tsunami data, the opportunity to deal with PTHA through a computational approach, involving the probability of all of the relevant sources and the numerical modeling of the generated tsunamis, which is in the scope of all the above-mentioned papers, is emphasized by several reviews (e.g., Geist and Lynett, 2014; Grezio et al., 2017).

Nevertheless, the computational procedure for a complete evaluation of PTHA, fully exploring the natural variability of the sources, can be extremely demanding and unfeasible in some cases, particularly when inundation calculations are involved for a target site (González et al., 2009; Geist and Lynett, 2014). This is due to the very large number of numerical simulations of tsunami generation, propagation and inundation on high-resolution topobathymetric models which is, in principle, required. For example, numerous realizations of heterogeneous slip are needed and usually obtained with stochastic procedures (LeVeque et al., 2016; Sepúlveda et al., 2017). Indeed, heterogeneous earthquake slip is known to strongly influence the tsunami run-up (Geist, 2002; Løvholt et al., 2012b; Geist and Oglesby, 2014; Davies et al., 2015; Murphy et al., 2016) and not only in the near-field of the source (Li et al., 2016). Among the first attempts to quantify tsunami hazard uncertainty related to heterogeneous earthquake slip, Mueller et al. (2014) and Griffin et al. (2017) should be mentioned. Recently, Goda and De Risi (2018) proposed a multi-hazard approach including stochastic slip distributions and cascading earthquake–tsunami risk evaluation; however, they considered a limited number of tsunami scenarios without fully characterizing the epistemic uncertainties associated with the key model components. Consequently, an efficient methodology is needed to make (onshore) PTHA a computationally affordable task.

The issue has been dealt with in various ways in several studies (González et al., 2009; Thio et al., 2010; Lorito et al., 2015; Lynett et al., 2016). In particular, Lorito et al. (2015) focused on seismic PTHA (SPTHA), that is, on hazards associated with tsunamis generated by coseismic seafloor displacement. They developed a method for significantly reducing the computational cost of the assessment, using a source-filtering procedure based on a cluster analysis. This allows for the identification of a subset of important sources able to preserve the accuracy of results. Furthermore, Selva et al. (2016) proposed a general procedure for the joint and unbiased quantification of aleatory and epistemic uncertainty, including the filtering procedure of Lorito et al. (2015) while stressing the importance of source completeness.

Here, we merge the two approaches of Lorito et al. (2015) and Selva et al. (2016), fully developing a method that enables the quantification of the local-scale SPTHA, and also devoting a large effort to refining the procedure and introducing several critical improvements. On the one hand, we modified the filtering procedure to enhance its computational efficiency and to adapt it to multiple sources covering a large range of source–target distances. On the other hand, to improve the accuracy we applied a separate treatment for remote and local sources, selecting near-field scenarios on the basis of the similarity of the coseismic tsunami initial conditions. This is crucial, as near-field sources may challenge the general assumption made by Lorito et al. (2015), where, for a given source, offshore tsunami amplitude profiles are considered representative of the coastal inundation behind them, regardless of the source location with respect to the coast. This was reasonable in that particular case study, since they considered either far-field scenarios with respect to the target coast or scenarios which deformed the coast in a definite direction; that is, the coast always subsided due to subduction earthquakes on the Hellenic arc. In the presence of more complex (and realistic) local fault distribution, causing either subsidence, uplift or mixed patterns depending on the case, tsunami intensity can be unpredictably reduced or enhanced with respect to the corresponding offshore tsunami wave (Mueller et al., 2014; Griffin et al., 2017). Hence, in general, offshore tsunami profiles could be strongly misleading when coseismic deformation of the coast occurs. This may affect the tail of the hazard curves in particular (i.e., largest intensities), to which local sources significantly contribute, as also demonstrated by the disaggregation analysis in Selva et al. (2016). For all of these reasons, special treatment is needed for local sources, based on the source similarities and considering the coseismic onshore displacement, rather than the offshore tsunami wave similarity.

For illustrative purposes, we considered a target site in the central Mediterranean as a use case, the Milazzo oil refinery (Sicily, Italy) in the southern Tyrrhenian Sea. This site was previously selected within the framework of the EU project STREST (http://www.strest-eu.org/, last access: 28 February 2019) as a test case for multi-hazard stress test development for nonnuclear critical infrastructure.

It is worth noting that this paper is strictly methodological and aims to propose a computationally efficient procedure for local-scale SPTHA, rather than provide a realistic site-specific hazard assessment. In fact, for the sake of simplicity and in order to not deflect attention from the core of the method, no efforts have been dedicated to constrain and test the (regional) seismic rates; the local seismic sources and their geometry and dynamics, including slip distributions; or the accuracy of topobathymetric data used in tsunami simulations. Moreover, the filtering procedure has been forced to minimize the number of explicit numerical simulations, allowing a relatively large accepted error with respect to the complete initial set of sources due to the introduced approximations.

The paper is organized as follows: Sect. 2 resumes the general outline of the method for SPTHA evaluation, as proposed by Lorito et al. (2015) and Selva et al. (2016), while the innovative developments are described in Sect. 3; Sect. 4 focuses on the illustrative application; conclusive remarks are drawn in Sect. 5.

Using regional-scale SPTHA as input for local-scale (site-specific) SPTHA, through the approach proposed by Lorito et al. (2015), is a task already foreseen by Selva et al. (2016) (see Fig. 1 therein). However, this possibility was neither applied nor tested in practice, since their main focus was the application for regional-scale analyses. The details of the general method have been already thoroughly described and validated in the previous studies. Here we will summarize the basic concepts.

The whole general procedure for site-specific SPTHA can be outlined in four steps: (1) the definition of earthquake scenarios and their probability, allowing, in principle, a full exploration of source aleatory uncertainty; (2) the computation, for each source, of tsunami propagation up to a given offshore isobath; (3) the selection of the relevant scenarios for a given site through a filtering procedure and the corresponding high-resolution tsunami inundation simulations; and (4) the assessment of local SPTHA with joint aleatory and epistemic uncertainty quantification by means of ensemble modeling, including modeling alternatives that were eventually implemented during steps (1)–(3).

In step (1), all the modeled earthquakes must be defined for different seismic regions, which are assumed to be independent of each other. The earthquake parameters and their logically ordered conditional probabilities are treated by means of an event tree technique. We emphasize that the common assumption that tsunami hazard is dominated at all timescales by subduction zone earthquakes is not used: non-subduction faults, unknown offshore faults, and diffuse seismicity around major known and well mapped structures are all taken into account. This strategy attempts to prevent biases in the hazard due to the incompleteness of the source model (Basili et al., 2013; Selva et al., 2016). The seismicity related to the main and better-known fault interfaces is treated separately to the rest of the crustal and diffuse seismicity. A similar approach has been used in the recent TSUMAPS-NEAM project (http://www.tsumaps-neam.eu/, last access: 28 February 2019), which provided the first SPTHA model for the northeastern Atlantic, Mediterranean and connected seas (NEAM) region.

In step (2), for each scenario retrieved from step (1) the corresponding
tsunami generation and propagation is numerically modeled, and the pattern of
offshore tsunami height above the sea level (*H*_{max}) is evaluated at a set
of points along the 50 m isobath in front of the target area. To provide
the input for Lorito et al. (2015), these points may be limited to a profile in
front of the site. The length of this control profile must be tuned depending
on the morphology and the extension of the target coast: a compromise has to
be reached, as too few points could make the profile not representative enough,
while too many points could downgrade the performance of the subsequent
filtering procedure (Lorito et al., 2015). Actually, the optimal length is the
shortest one that makes the offshore hazard curves stable with respect to the
source selection, and a further increase in length would increase the
computational effort without significantly altering the results.

In step (3), using the offshore *H*_{max} profiles calculated during step (2), a
filtering procedure is implemented to select a subset of relevant sources,
based on the similarity of the associated tsunami intensity and not on the
similarity or spatial proximity of the sources themselves. The selected
sources, each of them representative of a cluster of sources producing
comparable tsunamis offshore of the target area, are then used for explicit
inundation modeling on high-resolution topobathymetric grids. This approach
allows for a consistent and significant reduction of the computational cost
while preserving the accuracy. However, Lorito et al. (2015) considered a limited
set of sources. The extension to a much larger set of potential sources
requires some modifications to the method that, along with several other
improvements, are proposed in this study, as reported in Sect. 3.

Incidentally, we note that other wave properties, such as period or polarity, could be relevant in the framework of the cluster analysis. However, Lorito et al. (2015) briefly discussed this issue, also with respect to the length of the control profile, as discussed above. Nevertheless, this is a point probably deserving further investigation, considering that Satake et al. (2013) showed how inundation from the Tohoku 2011 tsunami was variably controlled by long-period offshore tsunami components on flat coastal plains and shorter-period peaks in steep coastal areas. Indeed, Gusman et al. (2014) used two cycles of a tsunami for identifying similar waves. Conversely, since, as described in the next section, offshore wave comparison is not used anymore in the near-field, this issue will not apply for local sources.

In step (4), local SPTHA is quantified. The inundation maps for each representative scenario from step (3) are aggregated according to the probabilities provided during step (1), assigning the total probability of a cluster to the representative scenario. Aleatory and epistemic uncertainty are simultaneously quantified by means of an ensemble-modeling approach (Marzocchi et al., 2015; Selva et al., 2016) over alternative implementations of the previous steps. In practice, steps (1) to (3) can be iterated for each alternative model, and these alternatives can be weighted according to their credibility and the possible correlation among the models. The results are finally integrated through ensemble modeling into a single model which expresses both aleatory and epistemic uncertainty.

The described method has been tested by both Selva et al. (2016) and Lorito et al. (2015). However, Lorito et al. (2015) focused on the filtering procedure of step (3), adopting a simplified configuration for the source variability, in which sources were allowed only within the Hellenic arc; that is, an area that is a source area too small to represent the full earthquake aleatory variability. On the other hand, Selva et al. (2016) applied the approach to a regional study that extended to the Ionian Sea in the central Mediterranean Sea. The quantification of the local hazard is instead discussed only in theory, without proposing any application.

The original method of Lorito et al. (2015) adopted a two-stage procedure.

In the first stage, scenarios giving a negligible contribution to *H*_{max}
offshore of the target area were removed, assuming they would lead to negligible
inundation. Hereafter, we call this stage “Filter H”.

As a second filtering stage, a hierarchical cluster analysis (HCA) was
carried out, separately for each earthquake magnitude class included in the
seismicity model, under the assumption that sources producing similar
offshore *H*_{max} along the control profile will also produce similar
inundation patterns. The distance (d) between two *H*_{max} patterns from two
different scenarios, *u* and *v*, was measured by a cost function previously
used to compare tsunami waveforms in source inversion studies
(e.g., Lorito et al., 2010; Romano et al., 2010) and modified by Lorito et al. (2015)
as follows:

where *x* runs over the control points of the 50 m isobath. For
each cluster, the scenario closer to the centroid was selected as the
reference scenario, with an associated probability corresponding to the
probability of occurrence of the entire cluster. The optimal number of
clusters (i.e., the “stopping criterion”) was assessed by analyzing the
variance within each cluster (hereafter, “intra-cluster”) as a function of
the number of clusters and selecting the largest value still producing
significant changes, according to the so-called Beale test (Lorito et al., 2015, and
references therein).

We implemented a different strategy to further reduce the number of explicit tsunami simulations and introduced a separate treatment for local and remote sources. In particular, the source scenario filtering procedure was revised to improve both the computational efficiency and accuracy, allowing for a full scalability to the source variability of typical SPTHA (millions of scenarios located all over an entire basin). A schematic diagram of the new procedure is sketched in Fig. 1, with (right, step 3b) or without (left, step 3a) the separation between near- and far-field.

We still kept Filter H but also adopted an additional filter on the
occurrence probability (hereafter, “Filter P”; see Fig. 1),
discarding scenarios whose cumulative mean annual rate (mean of the model
epistemic uncertainty) is below a fixed threshold. Filter P works as follows.
Scenarios are sorted according to their mean annual rate and the less frequent are
removed until the cumulated rate reaches the selected threshold. This allows
for a further reduction of the number of required numerical simulations. On the other
hand, this operation introduces a controlled downward bias to the estimated
hazard, whose upper limit corresponds (on average) to the probability
threshold of Filter P. This threshold can be set at a negligible level in
the framework of the overall analysis and/or with respect to other
uncertainties. In addition, it can be empirically checked as to what extent
this affects the results by analyzing the offshore hazard curves at the
control points. This check was quantitatively done by computing the maximum
deviation between the mean hazard curves at each control point before and
after Filter P was applied. We also notice that, as reported in Fig. 1, Filter P was always applied after Filter H due to strategic
reasons of optimization; in fact, the cumulated rate curve is lowered by the
removal of small events (i.e., producing small *H*_{max}), which
typically feature high-occurrence probability. As a consequence, a
greater number of scenarios can be removed before reaching the imposed
threshold, making Filter P more efficient.

Additionally, the cluster analysis stage was modified. Firstly, we used a different
algorithm, as the large number of source scenarios due to a realistic fault
variability distribution in some cases can make the HCA a computationally
unaffordable task. We implemented the more efficient *k*-medoids-clustering
procedure (Kaufman and Rousseeuw, 2009; Park and Jun, 2009) based on the minimization of the sum of
the intra-cluster distances, that is, the distances between each element of a
cluster and the cluster centroid. Strong constraints on the distances result
in a more accurate partitioning in terms of similarity among the elements of
each cluster but lead to a great number of clusters. Instead, larger ranges
of acceptability increase the efficiency of the algorithm, in terms of number
of resulting clusters, to the detriment of the accuracy. The cluster analysis
was performed separately for groups of scenarios with similar mean
$<{H}_{\mathrm{max}}>$ along the profile instead of grouping scenarios by earthquake
magnitude class. This makes the partitioning more efficient, as the
earthquake magnitude can not be considered the only parameter controlling the
tsunami intensity, as it was for the limited set of sources adopted by
Lorito et al. (2015). The cluster distance was measured by Eq. (1),
but we updated the stopping criterion, which is now related to the maximum
allowed intra-cluster variance, rather than being a blind optimization of the
number of clusters. More specifically, to control the dispersion within each
cluster, we set a threshold for the maximum allowed squared Euclidean
distance. This threshold was empirically fixed by comparing the offshore
hazard curves before and after the analysis and assuming an acceptable range
of variability, analogous to the approach used for Filter P.

Finally, and probably most importantly, in order to deal with the contribution from local sources properly, we implemented two independent filtering schemes for distant and local sources. Indeed, special treatment for near-field sources is needed, as the coseismic deformation can modify the actual local tsunami intensity at the nearby coast, due to coastal uplift or subsidence. As a consequence, the offshore tsunami amplitude profiles generated by such events may fail to be representative of the coastal inundation, and separate modeling is required using the coseismic deformation as the metric for source proximity in the cluster analysis (details below). This issue was somehow hidden in Lorito et al. (2015), due to the relatively small aleatory variability they considered being the source either in the far- or near-field, depending on the target site, but never mixed together. In addition, this separation may favor some refinement of the near-field source discretization and modeling, such as a denser sampling of geometrical parameters and/or the introduction of heterogeneous slip distributions.

For testing the proposed method, we replaced step (3) either with step (3a) or step (3b), as displayed in Fig. 1. The workflow of step (3a) is almost equivalent to the original procedure of Lorito et al. (2015) improved by the aforementioned changes related to the algorithm optimization, whereas the separate treatment of near- and far-field sources is included in step (3b). Step (3a) is then used in this study as a term of comparison for the new scheme.

In step (3a), three sequential tasks were performed, namely Filter H, Filter P and the cluster analysis based on the offshore tsunami amplitudes.

In step (3b), local and distant sources were firstly detected based on the coseismic deformation produced by the earthquake near and on the target coast. The procedure was then split into two parallel paths, which need to be merged at the end when evaluating SPTHA (Fig. 1). As far as the far-field scenarios are concerned, the same workflow as step (3a) was followed. Near-field scenarios, which, in principle, should be individually modeled, were also filtered in order to reduce the number of explicit inundation simulations: this of course introduces a new approximation, which, however, is better than aggregating local and remote scenarios on the basis of the offshore tsunami amplitudes. Filter H was applied as well, but a smaller threshold value was chosen: a more conservative approach is indeed recommended at this stage, as offshore values could be strongly misleading when significant coastal coseismic deformation occurs. Then Filter P was employed, and finally a cluster analysis was performed by comparing the coseismic deformations instead of the (unrepresentative) offshore tsunami amplitudes. For each local source, the vertical component of the coseismic displacement was calculated on a 2-D grid centered around the fault, which has a size equal to 3 times the fault length. Then the cluster analysis was carried out, separately for each magnitude, by comparing the coseismic fields point to point within the grid. In this case, the cluster analysis is based on the squared Euclidean distance instead of the cost function; the stopping criterion is also evaluated through the Euclidean distance, since the coseismic field can take both positive and negative values.

The selected earthquake scenarios from step (3a) or from the two branches (near- and far-field) of step (3b) were then used for high-resolution inundation simulations and combined together in step (4) when evaluating SPTHA. A practical example of the whole procedure is illustrated in the next section.

The described procedure was applied to a test site, Milazzo, located on the northeastern coast of Sicily, Italy, within the Mediterranean Sea. The site houses an oil refinery, one of the nonnuclear critical infrastructures selected as a case study in the framework of the EU project STREST (http://www.strest-eu.org/, last access: 28 February 2019).

Due to the illustrative purposes of the present work, some strong assumptions were imposed during the filtering procedure to drastically reduce the number of required explicit numerical simulations. The tuning of the filtering thresholds is not the objective of the present work; in fact, this application is aimed at highlighting that inaccurate (biased) evaluation of site-specific tsunami hazard would be obtained if scenarios located in the near-field of the target area are not properly taken into account, irrespective of the completeness and consequent complexity of the hazard assessment. However, more sanity and sensitivity tests would be mandatory for a finer tuning of thresholds and modeling in the case of a real application. For example, the modeling of near-field scenarios is expected to be dependent on the source parameters, especially concerning the heterogeneous slip distribution on the fault plane (e.g., Geist and Oglesby, 2014), which was not included here. Hence, the computational effort of a real assessment, including a wider source variability and more conservative thresholds, is expected to be more complicated and computationally demanding than this case study.

Regarding step (1), the adopted seismicity model was previously developed in
the framework of the EU project ASTARTE (http://www.astarte-project.eu, last access: 28 February 2019).
This model extends the method applied to the Ionian Sea in Selva et al. (2016) to
the entire Mediterranean Sea, including the subduction interfaces of the
Calabrian and Hellenic arcs as well as crustal seismicity in the whole basin
(see Fig. 2a). In subduction zones, events of different
magnitudes and positions over the whole interface are allowed, disregarding the geometry
uncertainty of the slab; conversely, crustal seismicity is allowed to occur
with any meaningful geometry and mechanism in the whole seismogenic volume at
different magnitudes and depths. The complete set of sources retrieved from
step (1) contains about 40 million elements, among which 1 701 341
scenarios actually affect the target site (*H*_{max}>0.05 m offshore
of Milazzo). Although relatively simplified, the source model also includes
epistemic uncertainties of many source parameters such as the seismic rates,
the shape of the magnitude–frequency distribution and the seismogenic depth
interval for the two subduction zones.

Tsunami amplitudes, step (2), were computed on a control profile made of 11 points offshore of the Milazzo target area (on the 50 m isobath), as reported in Fig. 2a. To save computational time, scenarios from step (1) were not individually simulated but were obtained by a linear combination of precalculated tsunami waveforms produced by Gaussian-shaped unitary sources (Molinari et al., 2016). The Gaussian propagation was modeled by the Tsunami-HySEA code, a nonlinear hydrostatic shallow-water multi-GPU code based on a mixed finite-difference–finite-volume method (de la Asunción et al., 2013; Macías et al., 2016, 2017).

Step (3) was addressed by independently performing the two branches (3a) and (3b), as discussed in the previous section, and then comparing results to assess the importance of the separate treatment of the near-field sources.

In step (3a), thresholds were fixed at 1 m for Filter H and 10^{−5} yr^{−1} for Filter P. This resulted in discarding scenarios with an individual
mean annual rate below $\sim {\mathrm{10}}^{-\mathrm{9}}$ yr^{−1}, causing a maximum bias in the
offshore mean hazard curves of about 10 % in the considered range of tsunami
intensities, with respect to the curves obtained without Filter P. At the end
of the filtering procedure, imposing a threshold equal to 0.2 on the
intra-cluster variance, we obtained 776 clusters, each associated with a
representative scenario. That is, we had a reduction above 99 %. Figure S1 in the Supplement shows the comparison among the mean offshore
hazard curves at the 11 control points, as well as among some quantiles of
the epistemic uncertainty, for the filtered and original set of scenarios.

It is worth stressing that the efficiency of the filters is artificially enhanced here by the imposed high thresholds, especially as far as Filter H is concerned. While 1 m is not an acceptable value in the case of a real hazard assessment, it is suitable for illustrative purposes. In any case, this filter, independently of the chosen threshold, is not expected to affect subsequent steps of the procedure for tsunami intensities above the threshold. Conversely, we performed a sensitivity analysis on the threshold imposed on the intra-cluster variance for the cluster analysis; Fig. S2 shows the percentage differences between the offshore hazard curves computed from the complete initial set of sources and the filtered set. The red box corresponds to the chosen threshold value (0.2): it appears evident that a smaller value would have allowed a stronger constraint on the error introduced by the cluster analysis while considerably increasing the number of resulting clusters. Vice versa, higher thresholds produce a smaller number of clusters but fail in reproducing the hazard (an error of up to 40 %). In the case of a real hazard assessment, this analysis would help in choosing an optimal threshold.

In step (3b), we considered as local scenarios, requiring separate
processing, sources that generate a coseismic vertical displacement greater than
or equal to 0.5 m on a set of near-field points; that is, the 11 control
points on the 50 m isobath plus 95 inland points strategically located at
the edges of the refinery storage tanks, as shown in Fig. 2b. We
found 4721 scenarios in the near-field (see Fig. 2a). Afterwards,
for both branches we applied Filters H and P as well, using the following
thresholds: for far-field scenarios, Filter H =1 m and Filter
P $=\mathrm{5}\times {\mathrm{10}}^{-\mathrm{6}}$ yr^{−1}; for near-field scenarios, Filter H =0.1 m,
according to the more conservative approach described in the previous
section, and Filter P $=\mathrm{5}\times {\mathrm{10}}^{-\mathrm{6}}$ yr^{−1}. Note that the Filter P threshold
was set to half of the value used in step (3a), in order to keep a total maximum
theoretical bias on the hazard curves at 10^{−5} yr^{−1}, as in step (3a),
considering that Filter P is separately applied both to far- and near-field
scenarios. Then the cluster analysis was carried out on the tsunami
amplitudes for far-field scenarios (using a threshold equal to 0.2 on the
intra-cluster variance) and on the coseismic deformation for near-field
scenarios (using a 10 % threshold for the intra-cluster variance). We
obtained 634 and 520 clusters for remote and local sources, respectively.
Thus, the total number of representative scenarios (1154) to be explicitly
modeled corresponds to a reduction of above 99 % of the initial set of sources.

Inundation simulations from step (3) were carried out again with the
Tsunami-HySEA code, exploiting the nested grid algorithm. We used four-level
nested bathymetric grids with a refinement ratio
equal to 4 and increasing resolution from 0.4 arcmin (∼740 m), to
0.1 arcmin (∼185 m), to 0.025 arcmin (∼46 m) and to
0.00625 arcmin (∼11 m). The largest grid was obtained by resampling
the SRTM15+ bathymetric model
(http://topex.ucsd.edu/WWW_html/srtm30_plus.html, last access:
28 February 2019). The three finest grids were
produced by interpolation from TINITALY (inland;
Tarquini et al., 2007, 2012) and EMODNET (offshore;
http://www.emodnet-bathymetry.eu/, last access: 28 February 2019) and working on grids of 0.00625 arcmin that were
resampled at 0.1 and 0.025 arcmin. A picture of the telescopic nested grids
is provided in Fig. S3. The initial conditions were differently provided for
subduction and crustal seismicity. The subduction scenarios were simulated by
modeling the slab as a 3-D triangular mesh honoring the interface
profile and using unitary Okada sources associated with each element of the
mesh (i.e., to each triangle) as Green's functions (Okada, 1985; Meade, 2007).
For crustal events, the initial sea level elevation was obtained by modeling
the dislocation on rectangular faults according to the Okada model. A
Kajiura-like filter for the sea bottom–water surface transfer of the
dislocation was also applied (Kajiura, 1963). For each simulation an overall
length of 8 h was fixed. The results were stored as maximum wave height
(*H*_{max}, m) and maximum momentum flux (MF_{max},
m^{3} s^{−2}) at each point of the inner (highest-resolution) grid.

During step (4), SPTHA was evaluated in parallel using results both from steps (3a) and (3b) in order to compare the outcomes of the two different workflows and estimate the impact of the special treatment of near-field sources on the site-specific hazard assessment. Note that alternative models for the epistemic uncertainty were only considered at step (1), that is, only as far as the probabilistic earthquake model is concerned, since the Selva et al. (2016) model was used.

Figures 3 to 5 compare the results from steps
(3a) and (3b) in terms of mean hazard curves and inundation (both
probability and hazard) maps for *H*_{max}. At first glance, differences
are appreciable in both the curves and the maps. It is worth noting that
results at *H*_{max}<1 m can be (negatively) biased since they are depleted
from the scenarios removed by Filter H, both in step (3a), as is clearly shown
in Fig. S1, and in the far-field branch of step (3b). Curves and maps will be
described in more detail below.

The hazard curves in Fig. 3a and b show the mean
(mean of the model epistemic uncertainty) exceedance probability over
50 years
for *H*_{max} (evaluated assuming a Poisson process, as in Selva et al., 2016),
plotted for each point of the finest-resolution grid. Panel (c) of the same
figure displays the one-by-one relative differences in terms of exceedance
probability (over 50 years), as a function of *H*_{max}, between the step (3a)
and (3b) curves at each grid point. For values of *H*_{max} greater than 1 m, the relative differences are systematically positive, meaning that
without the correction for near-field scenarios, step (3a), the tsunami
hazard would be overestimated. In Fig. S4 a sample of curves at a few inland points (one every thousand points) is displayed for
a direct curve-by-curve comparison between the two approaches. This confirms
that, overall, the uncorrected approach leads to hazard overestimation. We
may argue that this is true in the case of this specific setting, as a lower
“corrected” hazard means that the predominant effect of local sources
contributing to a specific point on the hazard curve is due to the coastal
uplift, which in turn decreases the tsunami hazard. For example, a cluster
may mix far- and near-field sources, which could be misrepresented by one
far-field source selected as cluster representative. In our case, there might
be a prevalence of clusters causing coastal uplift from the near-field
sources. The situation may be the opposite for a different source–target
configuration; that is, coastal subsidence could be predominant, causing an
hazard increase, which without correction could be underestimated. To confirm
our inference we performed some further testing. For each hazard intensity,
and only for the mean model of the epistemic uncertainty, we computed the
coseismic coastal displacement in the inner grid, averaged both over all of
the scenarios and over all of the coastal points (purple line in Fig. 3c). This quantity can be regarded as the mean uplift
(MU) on a random point on the coastline. Scenarios of different
types contribute to MU, both in far-field scenarios, which do not alter the
coastline, and in near-field scenarios, which may include a mixture of sources
producing both coastal subsidence and uplift. In more detail, we firstly
performed a weighted average of the coseismic displacements from each cluster centroid for each *H*_{max} with weights equal to the annual
probability of the individual earthquakes. These probabilities are set to
zero if the earthquake does not deform the coastline (i.e., for far-field
sources) or if the generated tsunami does not exceed the given *H*_{max}
value (i.e., that scenario does not contribute to the hazard at that point).
The weighted average is then normalized to the total probability of the near-
and far-field sources contributing to the tsunami hazard for that threshold.
The resulting MU on each coastal point is plotted for different values of
*H*_{max}≥1 m in Fig. S5 (blue lines). The
displacements due to the single cluster representatives are also shown (red
lines). We note that although single scenarios produce both positive and
negative coastal displacements, the predominant contribution is unveiled by
the sum of the different clusters, which is definitely positive. Additionally, for
higher intensities the contributing scenarios (decreasing in number, as
expected) generate displacements which are smaller and smaller, as important
uplift would significantly limit tsunami inundation. Finally, we further
averaged the resulting values along the coastline, obtaining the purple curve
in Fig. 3c. We notice that the absolute MU value in meters
turns out to be rather small as a result of the average over sources that
cause either uplift or subsidence, or no coastal displacement at all.
Regardless, the positive values obtained for *H*_{max}>1 m indicate that the uplift of
the coast is prevailing, consistent with the positive percentage
differences retrieved between the two approaches. Very little difference is
retrieved between the “corrected” and the “uncorrected” filtering
procedures for smaller values of *H*_{max}, that is, below the Filter H
threshold.

Finally, in Fig. 3d the relative differences are also shown
in terms of *H*_{max} as a function of exceedance probability (over 50 years). In
the low-probability region, typically corresponding to high *H*_{max}, the
overestimation by step (3a) is confirmed; conversely, for exceedance
probability greater than $\sim {\mathrm{10}}^{-\mathrm{4}}$, which is likely to correspond to
small *H*_{max}, a greater dispersion with both positive and negative values
is observed.

Probability and hazard inundation maps can be achieved by vertically and
horizontally cutting the hazard curves at chosen fixed values, in order to
give a geographical representation of results. As each hazard curve
corresponds to a grid point, the probability maps are obtained by plotting
all the probability values for a fixed value of the intensity metric on a
map. Instead, in the hazard maps the intensity values are plotted for a fixed
exceedance probability, corresponding to a given average return period (ARP). In
Fig. 4 we computed the exceedance probability maps for
*H*_{max}=2 m and *H*_{max}=3 m, while in
Fig. 5 we extracted the hazard maps for
$\mathrm{ARP}=\mathrm{2}\times {\mathrm{10}}^{\mathrm{5}}$ yr and $\mathrm{ARP}=\mathrm{3}\times {\mathrm{10}}^{\mathrm{5}}$ yr
(corresponding to an exceedance probability over
50 years equal to 2.5 and
$\mathrm{1.7}\times {\mathrm{10}}^{-\mathrm{4}}$, respectively).

For the selected values, the maps confirm what we already discussed about the
curves: mostly positive relative differences both inland and offshore are
inferred from the probability maps, as shown in Fig. 4c and
f, which are even larger than 50 %; these differences are positive at a
larger number of points for the higher intensity, consistent with
Fig. 3c. We recall that positive differences mean that the
“uncorrected” procedure, step (3a), actually overestimates the tsunami
hazard at the target site. Negative inland values are also observed for
*H*_{max}=2 m, but they occur for very low-probability values and
should not be further investigated. We also notice that the area inundated
with a non-negligible probability decreases in size when increasing the
*H*_{max} value as expected. In the hazard maps
(Fig. 5) a complex pattern is revealed when inspecting the
relative differences (panels c and f), as both positive and negative values
are retrieved. This happens because the analyzed ARPs lie in the
low-intensity range. The inundated area, opposite to the previous case, is
consistently more extended for larger ARPs.

Further details about the comparison can be found by analyzing the curves and
the maps for MF_{max} reported in Figs. S6 to S8. We merely note that, when the correction for near-field is taken into
account, the inundation maps highlight an enhanced current vorticity near the
docks (Figs. S7b, e and S8b, e), which is a known effect due to the flow
separation at the tip of a breakwater (Borrero et al., 2015). As the probability and
hazard maps aggregate several different sources, the hazard integral may tend
to average and cancel out different source effects while enhancing local
propagation features. The presence of such persistent physically meaningful
effects only in the maps retrieved using step (3b) confirms the importance of
the special treatment. In other words, the blind cluster analysis, step
(3a), exclusively based on the offshore tsunami amplitudes, likely produced
a nonrepresentative selection of the important scenarios, as it could
aggregate or even remove important local scenarios.

We proposed a computationally efficient approach to achieve robust assessment of site-specific SPTHA, developing an improved version of the method of Lorito et al. (2015) and Selva et al. (2016).

The procedure is based on four steps, which can be summarized as follows: (1) the definition of the set of earthquake scenarios and their mean annual rates, exploring the source aleatory uncertainty; (2) the computation of tsunami propagation up to an offshore isobath; (3) the implementation of a filtering procedure to select relevant scenarios for the target site, which are then explicitly modeled; and (4) the assessment of local SPTHA through an ensemble-modeling approach, to jointly quantify aleatory and epistemic uncertainty, stemming from alternative models for steps (1)–(3).

In the present work we focused on step (3), modifying the filtering procedure to enhance the computational efficiency and introducing a separate treatment for sources located in the near-field, to take into account the effect of the coseismic deformation on the tsunami intensity. To achieve this aim we implemented a new procedure including a correction for near-field scenarios and some numerical improvements. We benchmarked the new approach against an algorithm that is essentially equivalent to the original method of Lorito et al. (2015). The correction is crucial as the latter is based on the assumption that offshore tsunami profiles are representative of the inundation at the nearby coast, which might be true if a coseismic deformation of the coast is not involved; otherwise, seafloor uplift or subsidence make the assumption invalid. Consequently, local and remote sources must be separately treated by means of different filtering procedures. This may also allow for a specific and more detailed parameterization of the near-field sources, to which the local hazard is known to be more sensitive.

We tested the procedure by investigating a case study, i.e., Milazzo (Sicily). The work only has illustrative purposes and is not intended as a real hazard assessment at that site, due to some simplifications in the adopted model.

The new implemented filtering procedure allows for a consistent reduction of the number of tsunami inundation simulations and therefore of the computational cost of the analysis. It is worth stressing that in this specific application the computational efficiency was artificially enhanced by limiting the source variability, as well as by imposing high filter thresholds. In fact, a real assessment is expected to deal with a greater number of scenarios, provided that a finer tuning of the threshold values is carried out. This may in particular affect the computational cost related to the analysis of the near-field sources, for example when using stochastic slip distributions.

The most striking result is that the separate treatment of near-field sources
provides significantly different and physically more consistent results with
respect to the “uncorrected” procedure, showing that near-field sources
must be specifically dealt with when evaluating site-specific SPTHA. We
recall that the two approaches (with or without the correction for
near-field) only differ in the way local sources are treated. Hence, the
different results do not depend on the specific filtering thresholds but
only on the coseismic deformation induced by local sources, which, if properly
accounted for, modifies the effective tsunami hazard. Actually, for the
specific configuration of this use case, our findings reveal that not
considering an appropriate correction for near-field would lead to an
overestimation of the tsunami hazard for *H*_{max} greater than 1 m, and this
overestimation is correlated to dominant coastal uplift. However, different
cases in terms of overestimation and underestimation may occur at different sites,
depending on the relative source–site configuration. We also observe that
Milazzo is located in an area featuring relatively low near-field
tsunamigenic seismicity with respect to other areas in the Mediterranean Sea.
Nevertheless, the method turns out to be sensitive even to relatively low
displacements and allows for the detection and removal of significant biases from
near-field sources.

The proposed method is suitable to be applied to operational assessments and also for improving local (multi-hazard) risk analyses (e.g., Goda and De Risi, 2018). We stress again that the approach developed here allows for the consideration of a very high number of tsunami scenarios, which is necessary to sufficiently explore the natural variability of the tsunami sources and the eventual alternative models needed for quantifying epistemic uncertainty.

Future work will be devoted to the use of the procedure to perform real local hazard assessments, exploiting the regional hazard retrieved from the TSUMAPS-NEAM project.

The bathymetric data used for tsunami modeling are in the public domain and referenced in the text.

The regional hazard data are taken from Selva et al. (2016), as referenced in the text.

Hazard results are available upon request to the first author.

The supplement related to this article is available online at: https://doi.org/10.5194/nhess-19-455-2019-supplement.

MV, SL and JS elaborated the method and analysed the results; MV performed the analysis, included numerical simulations, and prepared the figures; MV and SL wrote the manuscript; RT and JS reprocessed data from regional hazard; FR gave support in preparing the numerical simulations and analyzing results; BB produced the bathymetric grids; all authors reviewed the manuscript.

The authors declare that they have no conflict of interest.

The authors want to thank the EDANYA Research Group at the University of
Malaga for providing the Tsunami-HySEA code for tsunami simulations. We
acknowledge useful discussions with William Power and Gareth Davies during
the early stages of this work. We also acknowledge constructive comments by
four anonymous referees, which allowed for
significant improvement of this paper. The work was partially funded by the
INGV–DPC Agreement (Annex B2) and by the STREST project, EC Seventh
Framework Programme (FP7/2007–2013), grant agreement no. 603389. All of the
figures were created using either MATLAB (https://www.mathworks.com/,
last access: 28 February 2019) or Generic Mapping Tools
(http://gmt.soest.hawaii.edu, last access:
28 February 2019).

Edited by: Maria Ana
Baptista

Reviewed by: four anonymous referees

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