On the calculation of smoothing kernels for seismic parameter spatial mapping: methodology and examples
Spatial mapping is one of the most useful methods to display information about the seismic parameters of a certain area. As in b-value time series, there is a certain arbitrariness regarding the function selected as smoothing kernel (which plays the same role as the window size in time series). We propose a new method for the calculation of the smoothing kernel as well as its parameters. Instead of using the spatial cell-event distance we study the distance between events (event-event distance) in order to calculate the smoothing function, as this distance distribution gives information about the event distribution and the seismic sources. We examine three different scenarios: two shallow seismicity settings and one deep seismicity catalog. The first one, Italy, allows calibration and showcasing of the method. The other two catalogs: the Lorca region (Spain) and Vrancea County (Romania) are examples of different function fits and data treatment. For these two scenarios, the prior to earthquake and after earthquake b-value maps depict tectonic stress changes related to the seismic settings (stress relief in Lorca and stress build-up zone shifting in Vrancea). This technique could enable operational earthquake forecasting (OEF) and tectonic source profiling given enough data in the time span considered.
The ultimate goal of operational earthquake forecasting (OEF) is to disseminate authoritative information using short-term time-dependent seismic hazards to help communities to prepare and manage damaging seismic emergencies. On the other hand, earthquake prediction aims to determine the future occurrence of a given earthquake from the observable behavior of earthquake-related parameters. Both approximations have to be given with corresponding uncertainties if the information is going to be used for further preventive action. Currently, the scientific community agrees with the hypothesis that the use of precursors has not yet provided a short-term seismic prediction framework (Uyeda and Nagao, 2018). However, in the ongoing research there is optimism on using OEF (Martinelli, 2020). Additionally, the integration of different seismic precursors in the OEF analysis might improve the reliability of the obtained results and help to improve the development of earthquake prediction systems in the future.
A seismic precursor is a phenomenon that takes place prior to the occurrence of an earthquake. There are several precursors, classified as seismic (anomalous seismicity and microseismicity, swarms and foreshocks, changes in b-value, hypocenter migration, changes in released energy and seismic waves velocities) and non-seismic (i.e., geophysical and/or geochemical precursors). Geophysical precursors can be electromagnetic field variations, ground resistivity, telluric currents, ground deformation and crustal movements, tilt and strain and in earth tidal strain, water level changes. Meanwhile geochemical precursors are related to radon and other gases emissions, and the chemical composition of underground water. These anomalous phenomena do not provide the basis for prediction of the three main parameters of an earthquake: place and time of occurrence and magnitude of the future seismic event but could forecast an increased probability of an imminent large earthquake occurrence. A more detailed review of earthquake precursors can be found in Cicerone et al. (2009).
Since the 1970s, when major efforts were made on promising precursors, such as radon and CO2 emissions, few advances have been achieved regarding earthquake precursors and how to develop a predictive model. However, on short time scales, less than a few months, earthquake sequences show a high degree of clustering in space and time. The probability of triggering increases with the magnitude and decay of the initial shock with elapsed time according to simple scaling laws. The first generation of models used for short-term clustering of earthquakes are the Omori law (Omori, 1984), Omori-Utsu law, also known as Modified-Omori law (Utsu, 1961, 1969), and then Reasenberg and Jones (1989), in chronological order.
The Gutenberg-Richter (Eq. 1, G–R from now on) empiric law (Gutenberg and Ritcher, 1956) has been and still is one of the most used mathematical models that aims to explain the magnitude-frequency earthquake distribution based on the observations compiled in the catalogs. The main reason for its popularity is its simple formulation, which in turn enables a more straightforward computer-based data process:
where a is the earthquake productivity for the area, b is related to the ratio between high magnitude and low magnitude earthquakes and NM≥m is the number of earthquakes with magnitudes M greater than a threshold magnitude, m.
The main constraint of this empiric law is that the catalog must describe a homogeneous Poisson point process, i.e., the process is random and the average number of events that occur per time unit, λ, is constant (irrespective of the length of the considered interval).
Recent studies have shown the importance of the so-called b-value regarding seismic risk assessment by relating low values (depending on the tectonic regime and the area) to tectonic stress build-up (Gulia and Wiemer, 2010). Moreover, the conclusions of this work agree with tests conducted in laboratory scale (Wiemer and Schorlemmer, 2007). Therefore, the relationship demonstrated by De Santis et al. (2019) between b parameter and the Shannon entropy has allowed the use of this thermodynamic variable as an indicator of the occurrence of an earthquake (Posadas et al., 2021, 2022); however, in addition, nonextensive entropy (Vallianatos et al., 2018; Vallianatos and Michas, 2020) is also likely to be used in the same terms (Papadakis et al., 2015). Finally, Galiana-Merino et al. (2022) proved the viability of using radon measurements to estimate the daily seismic activity rate. Then, time-dependent seismic hazard or risk can be computed using seismic and nonseismic information (e.g., radon) to provide useful results for OEF.
All the previous studies relied on an accurate estimation of the spatiotemporal variations of the b-value. They are discussed in the next part.
1.1 Temporal variations of the b value
The temporal distribution of earthquakes for a given tectonic region is usually used to evaluate the change of the b value before and after the occurrence of the main event in a certain area. The ability to monitor the seismic activity and the increase in the detection and characterization of the earthquakes in a certain area or fault is what makes this technique interesting.
The number of events used for the b-value estimation is a parameter that distinguishes two different methods: the rolling window method (RW) and the weighted likelihood method (WL).
The RW method has been used for a long time and can be seen in different studies (e.g., Gulia et al., 2016; Gulia and Wiemer, 2019; Smith, 1981). This method relies on the definition of an event window (considering a fixed number of events or for a certain period) for a stable b-value calculation. It is easy to implement and only requires a quick inspection of the temporal event distribution to determine the event window size.
The size of this window is often chosen arbitrarily, which means there may be a better choice or that the results may be not accurate in some windows. DeSalvio and Rudolph (2021) pointed out in their work that the traffic light system developed by Gulia and Wiemer (2019) for forecasting earthquakes with foreshocks higher than Mw≥6 should be evaluated with parameters obtained by optimization in the parameter space rather than handpicked values.
On the other hand, WL was introduced by Tormann et al. (2014) in order to eliminate the event window size choice (generally arbitrary) and has been used recently by Taroni et al. (2021a). It uses a time-decaying exponential weight function, which has been optimized by means of an exponential likelihood function. The main advantage of this method is that it avoids any arbitrary choice of parameters, so using different datasets with the same algorithm is enabled without previous event distribution studies.
1.2 Spatial distribution of the b value
The computation and mapping of the spatial distribution of the b value is a useful tool regarding information showcasing. Depending on the data and the level of detail it can help to describe structures such as faults or tectonic stress build-up zones (García‐Hernández et al., 2021).
There are several examples of b value spatial mapping due to shallow seismicity. Tormann et al. (2014) mapped the details of several faults from California (USA) and their tectonic stress distribution by developing a distance-dependent sampling method. Taroni and Akinci (2021) included foreshocks and aftershocks in the computations by means of a weighting function, so the catalog does not need to be declustered, although all the existing seismic series have to be identified. Additionally, depth profiles of the b-value spatial distribution are also useful for analyzing the tectonic behavior responsible of the intermediate and deep seismicity. Amongst others, Wiemer and Wyss (2002) computed the b-value in-depth changes to understand the seismic activity due to volcano-related seismicity. More recently, Batte and Rümpker (2019) used this technique to analyze the shallow seismicity and relate the high b values to heat flow in a rift environment. Chiba (2022) mapped the b-value distribution for the area from North Okinawa to Southern Kyushu Island (Japan), a region with a complex and rich tectonic setting, so the zones with more seismogenic potential are showcased.
When computing the spatial distribution of the b value, different smoothing kernels are used to weight down the events depending on the distance from the spatial grid cell in which the b value is calculated. The comparison between the event windows in the time series and the smoothing kernels can be made as they play the same role in the b-value calculation.
Another issue that has to be addressed is the method chosen for the estimation of the cut-off magnitude calculation. Recent work (Zhou et al., 2018) has shown that the characteristics of the seismic catalog determine which algorithm better suits the cut-off or threshold magnitude calculation which is needed to calculate the b value according to the maximum likelihood method proposed by Aki (1965) and improved by Utsu (1966).
Following the argument from the previous part regarding window sizes, the smoothing kernel should not be chosen arbitrarily, it is necessary to find a way to correlate the event distribution with the smoothing kernel. Therefore, we propose to correlate the epicenter spatial distribution of the events in the catalogs to determine the smoothing kernel to be used in the seismic parameter spatial mapping. The function that best describes the spatial distribution of the events of the catalog is also the best to approach neighboring events when calculating the b value in a given spatial cell.
Smoothing kernels in spatial mapping
According to the definition of the weighting functions, the parameter σ (Brunsdon et al., 2002), regarded as a band width, determines the focus or level of detail, so the higher this parameter, the slower this smoothing kernel function decays over space and vice versa. This means that the lower σ values, the higher level of detail.
Recently, Taroni et al. (2021b) refined the Tormann et al. (2014) methodology to plot the spatial distribution of the b value in Italy, and although there exists controversy in the conclusions (Gulia et al., 2022), our main interest is the methodology and the event catalog. They employed the σ value calculated by Murru et al. (2016), by means of the maximization of the likelihood of the seismicity contained in half of the parametric catalog of the historical Italian earthquakes (CPTI15 – Release v1.5-July 2016 – from Rovida et al., 2020) and obtained a smoothing parameter of 30 km for central Italy.
One of the main weaknesses of the non-epidemic type aftershock sequence (ETAS) b-value spatial mapping current methodologies, is the fact that there is no clear justification for the use of the smoothing kernel function based on the event spatial grid cell distance for regional b-value mapping. Both the spatial grid cell size and resolution are arbitrary and do not provide information of the seismic sources of the zone, as the only purpose of the grid's extent is to contain all the events of the catalog. Although the influence of the grid choice can be minimized as pointed out by Tormann et al. (2014), this distance distribution does not relate to each event's source. We introduce a methodology that relies on the analysis of the event-event distance distribution for the fit of the smoothing kernel function and its parameters in order to optimize the resolution of b-value mapping.
In order to obtain the smoothing kernel function and its parameters for a given seismic catalog, we follow the next steps.
First, it is necessary to study both the event-event distance and the spatial cell-event distance distribution. The event-event distance is the distance between any two events of the catalog (in any of the case studies the distances between all the event pairs are calculated), as for the spatial cell-event distance, it is defined as the distance between a spatial grid cell and an event from the catalog (as in the former definition the distances between all the spatial cells and all the events are calculated). These quantities can be calculated once the Euclidean coordinates are obtained for each event and the spatial cell of the grid (Eq. 2):
where d is the Euclidean distance, x is the abscissa and y is the ordinate of each point (event or center of the spatial cell).
The main problem regarding this step arises when the catalogs are extensive. The number of events can increase the memory requirements for the event-event distance calculation, as for each event it is necessary to calculate as many distances as events exist in the catalog. For example, if the catalog has 50 000 events it is necessary to allocate enough memory to store a 50 000×50 000 float-type array. This can also happen when calculating the spatial cell-event distance distribution depending on the area’s size or the spatial cell resolution.
There are several ways to work around this situation. If the area does not display many seismic clusters, i.e., the distribution of the events can be approximated as a random one, then a set of random events in the catalog can be used to calculate the distance distribution instead of the full catalog. For this condition to be fulfilled, the area should be sized so no tectonic features (around which the events may cluster) have influence on the seismic record. Another option is to split the catalog into several parts when the previous condition cannot be fulfilled. Tormann et al. (2014) proposed the introduction of a cut-off distance for the calculation of the spatial cell-event distance-based weighting function values. According to their work, the events further than 7.5 km away have no influence on the outcome so they can be ignored. To avoid the loss of resolution and stability they also include a minimum number of events for each spatial cell.
In our case, the same catalog as Taroni et al. (2021b) is used initially and all the events of the catalog are considered for each spatial cell b-value calculation. Instead of using a cut-off distance, the influence of the events in the b-value calculation is controlled by means of the smoothing kernel and its parameters.
Once the distances have been calculated the next step is to plot these results and analyze them. If the distance distribution can be fitted to a function, then the smoothing kernel parameters is obtained as a result of this fit. For example, if the distance distribution is identified as a normal distribution, then σ is calculated as the second moment of the distribution (the variance).
Lastly, the weighting function that controls the influence of the events on the b-value calculation should be defined. In this case, it is the result of the product of two components: the fitted function that plays the role of the smoothing kernel and then a function that controls the weighting of the events that belong to a seismic series following the procedures of Taroni and Akinci (2021). The final weighting function can be defined as follows (Eq. 3):
where WSK is the smoothing filter and WSS is the function used to add foreshocks and aftershocks into the b-value calculation.
where N is the total number of events in the catalog, M is the magnitude of the event, Mmin is the threshold magnitude and Δ is the binning of the magnitude in the catalog. In these case studies the threshold magnitude does not change in a manner that can affect the b-value calculation, so no changes depending on time windows have been considered.
The uncertainty of this b-value has been calculated following the procedure of Taroni et al. (2021b) and it was derived by these authors following the work of Aki (1965) and applying the delta method (Dorfman, 1938) to take into account the weighting function used in the b-value calculation:
The influence of the choice of the smoothing kernel is important, which is why it should be made by means of a function fit. Figure 1 depicts the difference between several functions used as smoothing kernels and the weight each event is given depending on the distance (between the event and another event of the catalog or the event and a given spatial cell).
Our methodology is first be validated using the calibration catalog for Italy (Taroni et al., 2021b) and then applied to two different seismic environments: Lorca (southeast Spain) in the time span around the main earthquake in the last decades (the 2011 Lorca's earthquake Mw 5.1) and the Vrancea region (center of Romania), in a period of time also including two earthquakes of Mw higher than 5. The Lorca region is dominated by shallow crustal earthquakes while the Vrancea region is mainly guided by intermediate and deep seismicity.
3.1 Calibration catalog: Italy
The Italian catalog comprises the events from 1960 to 2019 for all Italy. It amounts to 56 309 events, which can be described in terms of magnitude and depth. The depth of the events ranges from 0 to 30.0 km, so the seismicity considered for this area is shallow (this catalog has been filtered so no aftershocks, foreshocks or events with a depth greater than 30 km appear). As for the magnitudes, the minimum is Mw 1.81 and the maximum is Mw 6.81. All the events can be displayed in a frequency-magnitude plot in order to examine their distribution (Fig. 2).
First, the distance between the ith event with the rest of the catalog and between the jth spatial cell and the events of the catalog are computed (). These quantities are called event-event distances and spatial cell-event distance from now on.
In Fig. 3, it can be seen that the spatial cell-event distance does not give useful information as the distance distribution is the same for each period and it only depends on the shape of the grid and point density. For this reason, this quantity is not considered in further case studies.
The event-event distance distribution shown in Fig. 4 can be fitted to a different function depending on the period, but it is important to compare the number of counts in each histogram to draw further conclusions. For the period from 2016 to 2017 it can be seen that for each bin of the histogram the counts are one order of magnitude higher than for the rest of the periods. This means that this distance distribution is representative of the catalog except for the distances further than 50 km (for which the counts are lower and the influence of the other histograms when summed can modify the distribution).
All the histograms have been stacked so the event-event distance distribution can be studied (Fig. 5).
In order to obtain the smoothing kernel, two functions have been considered based on the existing literature for the exponential-like function (Tormann et al., 2014) and mathematical significance for the Gaussian kernel as this function has a direct relationship with the distance distribution by means of the μ and σ parameters. First, the Gaussian function (Eq. 6):
where A is the normalization constant, μ, is the mean value or first moment of the distribution (the maximum value of the Gaussian function) and σ is the standard deviation or second moment of the distribution. These are the parameters obtained by fitting the data to this model, although the mean value is usually set to zero or the data are normalized to impose a zero-mean value for simplicity (Rasmussen and Williams, 2006).
where r is the distance and c and d are both real parameters that are adjusted using the test data shown in Fig. 5. For this function to be fitted, the count distribution has been normalized by dividing the counts of each bin by the sum of counts in all the bins so that the parameters can be used for the weight function calculation without the need of a normalization constant.
The exponential-like function is a better fit for the event-event distance distribution as can be seen in both Fig. 6 and Table 1, where the correlation coefficient, a measure of how much the points of the model function differ from those of the dataset, R2, is closer to 1 for the exponential-like function.
Only the spatial cell grids where the b-value is in the 95 % confidence interval (CI) with that of Taroni et al. (2021b) are plotted (only 10 spatial cells out of 4074 were outside the 95 % CI). The difference between the two spatial maps is lower than 2 % in most of the country except for border areas in which the difference can rise up to a 15 % as can be seen in Fig. 7. This can be due to less data being available for the b-value calculation (border effect).
Once the proposed methodology to obtain the smoothing kernel value in order to compute the b-value spatial distribution has been tested, it is applied to two different case studies.
3.2 Case study: Lorca and Vrancea regions
3.2.1 Lorca region (Spain)
For the area of Lorca, we select the following region centered around the epicenter of the Lorca earthquake that happened on 11 May 2011 at 16:47 UTC. This event has been extensively studied. For instance, Martinez-Diaz et al. (2012) studied the rupture of the Alhama de Murcia fault and calculated the stress build-up and release using different fault models by means of interferometry data to account for the co-seismic deformation. González et al. (2012) studied the relationship between the crustal stress changes and the co-seismic slip distribution. Frontera et al. (2012) performed a comparison of the deformation by means of data and numerical models. More information about the Lorca earthquake can be found in the special issue of the Bulletin of Earthquake Engineering (Alarcón and Benito, 2014).
In order to apply the proposed methodology, a part of the Spanish earthquake catalog (https://www.ign.es/web/ign/portal/sis-catalogo-terremotos, last access: 26 June 2022) was filtered selecting the events in a 40 km radius circumference centered at the Lorca earthquake epicenter. Events have been selected from years 2000–2021 to have enough events to calculate the b-value (Fig. 8). This catalog has a total of 2962 events with magnitudes between Mw 0.8 and Mw 5.0 (low to moderate earthquakes) and depths that range from 0 to 32.0 km (shallow seismicity). Before November 1997, epicentral location uncertainties were calculated with Hypo71 (Lee and Lahr, 1975) and specified as the so-called standard horizontal error (SHE in km). However, since November 1997, epicentral location uncertainties calculated by Evloc (Carreño-Herrero and Valero-Zornoza, 2011) are reported as error ellipses at the 90 % confidence level in the full format catalog. The epicentral location and the focal depth has uncertainties usually lower than 5 km within the Iberian Peninsula (González, 2017).The threshold magnitude for shallow seismicity is Mw 1.8.
The catalog has been divided in two parts: a pre-series period (from 2000 to 2011) and a post-series period (from 2011 to 2020) so that the b-value maps can be studied. Following the procedure described in the former example, the event-event distributions have been plotted and the two functions presented before being fitted in order to obtain the smoothing kernel function and its parameters. The clusters have been identified by means of the Reasenberg and Jones (1989) algorithm.
Then, Fig. 9 represents the event-event distance distribution. As can be seen there is no clear distribution for the 0–80 km interval in the first period, panel (a). However, the extension of the area allows considering only the first 14 km of the distance distribution. The Gaussian function has been fitted in panel (b) with this constraint. As for the exponential function all the data have been used. For the second period (2011–2020) the event-event distance distribution in panel (c) shows a clearer tendency for this reason and the functions that have been fitted in panel (d) use all the available data. The parameters obtained are presented in Table 2.
It can be seen in both Fig. 9 and Table 2 that the Gaussian function is a better fit for the event-event distance distribution. Then, using this smoothing kernel the b-value distribution for both periods is plotted.
Figure 10a shows that the b-values in the proximity of the fault responsible of the Lorca earthquake (in the center of the circle) are lower than the tectonic zone's mean value (b = 1.03, García-Mayordomo et al., 2012). As this part of the catalog comprises the 10 years before the Lorca earthquake, the b-value spatial distribution calculated shows a zone of increased tectonic stress in the NE and SW parts of the fault, before the main Lorca series event.
In Fig. 10c it can be seen that the b-values are higher than the average value cited before. This could imply that part of the tectonic stress build-up has been released by means of the earthquakes of the Lorca series.
3.2.2 Vrancea region (Romania)
The Vrancea region, 135 km distant from Romania's capital, Bucharest, is one of the zones with the highest seismic activity in Europe. Historical records of earthquakes show evidence of events with Ms higher than 7 (the earthquakes from 1802 and 1838) and recent events (1990s) have reached Mw higher than 6 (Zaicenco et al., 2008).
It is noteworthy to highlight that all strong earthquakes registered have occurred at depths greater than 60 km, which have become the focus of research for this zone. The up to date catalog of Romania can be found at the following address: http://www.infp.ro/index.php?i=romplus (last access: 26 June 2022). Between 1990 and the end of 2013, locations were determined using the HYPOPLUS (Oncescu et al., 1996) program, a 1D velocity model and stations corrections. Starting in 2014 the earthquake location is obtained using Antelope software. In the present form, a single magnitude scale (Mw moment magnitude scale) is adopted for all events. Different magnitude scales used before 2014 were converted into moment magnitude (Mw), based on calibration relations presented in the work by Oncescu et al. (1999).
Taking into consideration that the region has suffered 2 earthquakes with Mw 5.5 in the last decade, we have chosen the events from 2000 to 2018 in the Vrancea region. The b-value mapping area is enclosed by the blue frame in Fig. 11, in which all the events of the catalog for this period are shown.
The catalog contains 6615 events with magnitudes ranging from Mw 0.1 to Mw 6.0, 35 % have shallow depth, 19 % have intermediate depth and 46 % have deep depth. As can be seen most (65 %) are intermediate and deep seismicity. The cut-off magnitude for this catalog is Mw 2.70.
The events can be plotted in the frequency-magnitude graph depending on the depth. In this case deep seismicity accounts for intermediate and deep events (>50 km depth) and shallow seismicity for those with depth less than 50 km. In this case, the catalog has not been filtered prior to calculation (the Italian and Spanish only contain shallow seismicity; hence they do not require a G-R fit to discriminate the different seismic settings).
Figure 12 represents the frequency-magnitude distribution of the earthquakes at different depths and the tendency of the G-R law. A b-value of 2.00 for the shallow seismicity has been found and a b-value of 0.91 has been calculated for the deep seismicity. The different slopes indicate that separate catalogs should have been used to compute the spatial b-value distribution for each depth range. As the moderate to large earthquakes have a depth greater than 50 km, only intermediate and deep seismicity are considered for the study.
In this zone two major earthquakes occurred: on 23 September 2016, 23:11 UTC and 28 October 2018, 00:38 UTC. The catalog is split into two parts: from 2000 to 2016, and from 2016 to 2018 (both periods before the respective earthquakes happened) in order to compare the b-value spatial distribution. The first step is to calculate the event-event distance distribution as in the previous cases (Fig. 13).
Both of the functions seem to fit the data, although the Gaussian function overestimates the distribution in the first kilometers and the exponential function overestimates the last kilometers. The parameters obtained by means of the functions fit are provided in Table 3.
Both functions are compared. First, the Gaussian function is used as the smoothing kernel (Fig. 14).
As can be seen in Fig. 13b and c the fit of the Gaussian function in the first 10 km is not optimal. Therefore, the exponential-like function, which fits better at the first kilometers of the event-event distance distribution, can be used to compare the results (Fig. 15).
The b-value maps in Figs. 14c and 15c when compared with those in Figs. 14a and 15a enable identification of an increase in the b-value near the epicenter of the earthquake of 2016 which could indicate tectonic stress relief and a slight b-value decrease towards the SW part of the area. This shifting could account to the tectonic stress build-up preceding the 2018 earthquake. The main difference between the exponential function and the Gaussian function when used as spatial kernels in this case is the level of detail and the b-value range (difference between the maximum and minimum values). This can be explained by examining the graphs of the exponential function fit in Fig. 13b and d. The decay in the exponential function is faster than the Gaussian function, so the influence of weighting function in the b-value calculation is less for the most remote events in the exponential function than it is in the Gaussian function.
This method for the smoothing kernel assessment and the calculation of its parameters is able to obtain results compatible with those obtained by different methods (likelihood function). Moreover, it avoids the arbitrary selection of a smoothing kernel by fitting a function to the distance distribution and obtaining the parameters for it.
Although the spatial cell-event distance histogram has been shown for comparison purposes, it serves no use for the spatial kernel function calculation as the spatial grid is arbitrary (both in its extension and resolution) and the only constraint for this grid is to cover the entire area in which the events of the catalog are located.
It is illustrative to use the Gaussian function as the fit for the event-event distribution as it is a well-known function with parameters that can be easily related to the event-event distance distribution and its characteristics. Nevertheless, other distributions can be considered as long as the function that describes them is compatible with the data as shown in the Vrancea region case study.
Another interesting topic that can be addressed is the relationship between the σ value in the case of the Gaussian function (as it is directly related with the event distribution) and the fault distribution in the study area, in case one exists, as it could enable tectonic structure profiling.
The use of different parts of the catalog in order to describe the b-value spatial distribution as time passes can enable OEF as long as there are enough data for it to be stable. We used parts of the catalog before and after a major earthquake, but it could be used to describe yearly (or even monthly depending on the zone) b-value changes.
The data and code used in this study are available upon request.
DML and SM developed the original idea. JJGM and IGD helped in the development of the methodology. DML and SM performed the data curation. DML wrote the code and tested the different components. All the co-authors participated in the investigation and interpretation of the results. DML prepared the original draft, and SM, JJGM and IGD reviewed and edited it.
The contact author has declared that none of the authors has any competing interests.
Publisher’s note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
We want to thank Research Group VIGROB-116 (University of Alicante) and Stefan-Florin Balan, Victorin-Emilian Toader and Iren-Adelina Moldovan from the National Institute for Earth Physics (Romania) for the provided data and comments.
This research has been supported by the Horizon 2020 (TURNkey (grant no. 821046)) and the Ministerio de Ciencia e Innovación (grant no. PID2021-123135OB-C21).
This paper was edited by Filippos Vallianatos and reviewed by two anonymous referees.
Batte, A. G. and Rümpker, G.: Spatial mapping of b-value heterogeneity beneath the Rwenzori region, Albertine rift: Evidence of magmatic intrusions, J. Volcanol. Geoth. Res., 381, 238–245, https://doi.org/10.1016/j.jvolgeores.2019.05.015, 2019. a
Brunsdon, C., Fotheringham, A., and Charlton, M.: Geographically Weighted Summary Statistics—A Framework for Localised Exploratory Data Analysis, Comput. Environ. Urban, 26, 501–524, https://doi.org/10.1016/S0198-9715(01)00009-6, 2002. a
Carreño-Herrero, E. and Valero-Zornoza, J. F.: The Iberian Peninsula seismicity for the instrumental period: 1985–2011, Enseñ. Cienc. Tierra, 19, 289–295, 2011. a
Chiba, K.: Heterogeneous b-value Distributions Measured Over an Extensive Region from the Northern Okinawa Trough to Southern Kyushu Island, Japan, Pure Appl. Geophys., 179, 899–913, https://doi.org/10.1007/s00024-022-02958-5, 2022. a
De Santis, A., Abbattista, C., Alfonsi, L., Amoruso, L., Campuzano, S. A., Carbone, M., Cesaroni, C., Cianchini, G., De Franceschi, G., De Santis, A., Di Giovambattista, R., Marchetti, D., Martino, L., Perrone, L., Piscini, A., Rainone, M. L., Soldani, M., Spogli, L., and Santoro, F.: Geosystemics View of Earthquakes, Entropy, 21, 412, https://doi.org/10.3390/e21040412, 2019. a
Dorfman, R.: A note on the δ-method for finding variance formulae, Biometrics Bull., 1, 129–137, 1938. a
Frontera, T., Concha, A., Blanco, P., Echeverria, A., Goula, X., Arbiol, R., Khazaradze, G., Pérez, F., and Suriñach, E.: DInSAR Coseismic Deformation of the May 2011 Mw 5.1 Lorca Earthquake (southeastern Spain), Solid Earth, 3, 111–119, https://doi.org/10.5194/se-3-111-2012, 2012. a
Galiana-Merino, J. J., Molina, S., Kharazian, A., Toader, V.-E., Moldovan, I.-A., and Gómez, I.: Analysis of Radon Measurements in Relation to Daily Seismic Activity Rates in the Vrancea Region, Romania, Sensors, 22, 4160, https://doi.org/10.3390/s22114160, 2022. a
García-Mayordomo, J., Insua-Arévalo, J., Martinez-Diaz, J., Jiménez-Díaz, A., Martín Banda, R., Alfageme, M., Álvarez Gómez, J., Rodríguez-Peces, M., Perez-Lopez, R., Rodriguez-Pascua, M., Masana, E., Perea, H., Martín-González, F., Giner-Robles, J., Nemser, E., Cabral, J., Sanz de Galdeano, C., Peláez, J., Tortosa, G., and Linares, R.: The Quaternary Active Faults Database of Iberia (QAFI v.2.0), J. Iber. Geol., 38, 285–302, 2012. a, b, c
García‐Hernández, R., D'Auria, L., Barrancos, J., Padilla, G. D., and Pérez, N. M.: Multiscale Temporal and Spatial Estimation of the b‐Value, Seismol. Res. Lett., 92, 3712–3724, https://doi.org/10.1785/0220200388, 2021. a
González, P., Tiampo, K., Palano, M., Cannavò, F., and Fernandez, J.: The 2011 Lorca earthquake slip distribution controlled by groundwater crustal unloading, Nat. Geosci., 5, 821–825, https://doi.org/10.1038/ngeo1610, 2012. a
Gulia, L., Tormann, T., Wiemer, S., Herrmann, M., and Seif, S.: Short-term probabilistic earthquake risk assessment considering time-dependent b values, Geophys. Res. Lett., 43, 1100–1108, https://doi.org/10.1002/2015GL066686, 2016. a
Gulia, L., Gasperini, P., and Wiemer, S.: Comment on “High‐Definition Mapping of the Gutenberg–Richter b‐Value and Its Relevance: A Case Study in Italy” by M. Taroni, J. Zhuang, and W. Marzocchi, Seismol. Res. Lett., 93, 1089–1094, https://doi.org/10.1785/0220210159, 2022. a
Gutenberg, B. and Ritcher, C. F.: Magnitude and energy of earthquakes, Ann. Geophys., 9, 1–15, 1956. a
Lee, W. H. and Lahr, J. C.: HYPO71 (revised): a computer program for determining hypocenter, magnitude, and first motion pattern of local earthquakes, Open-File Report 75-311, U.S. Dept. of the Interior, Geological Survey, National Center for Earthquake Research, https://doi.org/10.3133/ofr75311, 1975. a
Martinez-Diaz, J., Bejar, M., Álvarez Gómez, J., Mancilla, F. d. L., Stich, D., Herrera, G., and Morales, J.: Tectonic and seismic implications of an intersegment rupture: The damaging May 11th 2011 Mw 5.2 Lorca, Spain, earthquake, Tectonophysics, 546–547, 28–37, https://doi.org/10.1016/j.tecto.2012.04.010, 2012. a
Omori, F.: On the aftershocks of earthquakes, Journal of the College of Science, 7, 111–200, 1984. a
Oncescu, M. C. and Marza, V. I., Rizescu, M., and Popa, M.: The Romanian Earthquake Catalogue Between 984 – 1997, Springer Netherlands, Dordrecht, 43–47, https://doi.org/10.1007/978-94-011-4748-4_4, 1999. a
Oncescu, M. C., Rizescu, M., and Bonjer, K.-P.: SAPS—An automated and networked seismological acquisition and processing system, Comput. Geosci., 22, 89–97, https://doi.org/10.1016/0098-3004(95)00060-7, 1996. a
Papadakis, G., Vallianatos, F., and Sammonds, P.: A nonextensive statistical physics analysis of the 1995 Kobe, Japan earthquake, Pure Appl. Geophys, 172, 1923–1931, https://doi.org/10.1007/s00024-014-0876-x, 2015. a
Posadas, A., Morales, J., and Posadas-Garzon, A.: Earthquakes and entropy: Characterization of occurrence of earthquakes in southern Spain and Alboran Sea, Chaos, 31, 043124, https://doi.org/10.1063/5.0031844, 2021. a
Posadas, A., Morales, J., Ibañez, J., and Posadas-Garzon, A.: Shaking earth: Non-linear seismic processes and the second law of thermodynamics: A case study from Canterbury (New Zealand) earthquakes, Chaos Soliton. Fract., 151, 111243, https://doi.org/10.1016/j.chaos.2021.111243, 2022. a
Smith, W. D.: The b-value as an earthquake precursor, Nature, 289, 136–139, 1981. a
Taroni, M. and Akinci, A.: A New Smoothed Seismicity Approach to Include Aftershocks and Foreshocks in Spatial Earthquake Forecasting: Application to the Global Mw≥5.5 Seismicity, Applied Sciences, 11, 10899–10910, https://doi.org/10.3390/app112210899, 2021. a, b
Taroni, M., Zhuang, J., and Marzocchi, W.: High-Definition Mapping of the Gutenberg–Richter b-Value and Its Relevance: A Case Study in Italy, Seismol. Res. Lett., 92, 3778–3784, https://doi.org/10.1785/0220210017, 2021b. a, b, c, d, e, f, g, h, i
Tormann, T., Wiemer, S., and Mignan, A.: Systematic survey of high-resolution b value imaging along Californian faults: Inference on asperities, J. Geophys. Res.-Sol. Ea., 119, 2029–2054, https://doi.org/10.1002/2013JB010867, 2014. a, b, c, d, e, f, g
Utsu, T.: A statistical study on the occurrence of aftershocks, Geophysical Magazine, 30, 521–605, 1961. a
Utsu, T.: A method for determining the value of b in a formula log n=a-bM showing the magnitude frequency relation for earthquakes, Geophys. Bull. Hokkaido Univ., 13, 99–103, 1965. a
Utsu, T.: A Statistical Significance Test of the Difference in b-value between Two Earthquake Groups, J. Phys. Earth, 14, 37–40, 1966. a
Utsu, T.: Aftershocks and earthquake statistics (1): Some parameters which characterize an Aftershock sequence and their interrelation, Journal of the Faculty of Science, Hokkaido University, 3, 129–195, 1969. a
Uyeda, S. and Nagao, T.: International cooperation in pre-earthquake studies: History and new directions, in: Pre-earthquakes processes. A multidisciplinary approach to earthquake prediction studies, edited by: Ouzounov, D., Pulinets, S., Hattori, K., and Taylor, P., John Wiley & Sons Sons, 3–6, https://doi.org/10.1002/9781119156949.ch1, 2018. a
Vallianatos, F. and Michas, G.: Complexity of Fracturing in Terms of Non-Extensive Statistical Physics: From Earthquake Faults to Arctic Sea Ice Fracturing, Entropy, 22, 1194, https://doi.org/10.3390/e22111194, 2020. a
Vallianatos, F., Michas, G., and Papadakis, G.: 2 - Nonextensive Statistical Seismology: An Overview, in: Complexity of Seismic Time Series, edited by: Chelidze, T., Vallianatos, F., and Telesca, L., Elsevier, 25–59, https://doi.org/10.1016/B978-0-12-813138-1.00002-X, 2018. a