Simplified twodimensional modelling to constrain the deep groundwater contribution in a complex mineral water mixing area, Riardo Plain, southern Italy
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Abstract
Complex hydrogeological systems require detailed knowledge of aquifer dynamics to ensure appropriate and sustainable management of the groundwater resource. The Riardo Plain aquifer, southern Italy, is a strategic resource for conjunctive uses; nevertheless, the conceptual model still suffers some uncertainties due to the presence of a deep lateral inflow through the carbonate basement. Therefore, the realisation of a 3D numerical model at catchment scale needs preliminary tests to constrain the possible additional inflow rate, which is at the moment only estimated through the results of the groundwater budget calculation. A 2D section of the mixing area was modelled using FEFLOW in order to test the hypothesis of a combined recharge. Seven versions of the same model were calibrated over an increasing number of adjustable parameters according to their sensitivity. The most efficient model version was identified according to the calculated information criteria and the sum of squaredweighted residuals. In the second phase of the work, nine model scenarios characterised by different deep inflow rates were calibrated and validated according to the same procedure of the first model, in order to identify the range of possible acceptable solutions. The most likely deep inflow rate is 34 ± 4% of the total recharge, corresponding to an estimated deep inflow of 415 ± 50 L/s in the Riardo Plain aquifer through the carbonate basement. This methodological approach will be the basis of following numerical 3D numerical models of the Riardo Plain and can be a valuable tool in conceptualising similar mineral water areas.
Keywords
Numerical modelling Mineral aquifer FEFLOW Parsimonious models ItalyModélisation bidimensionnelle simplifiée pour limiter la contribution des eaux souterraines profondes dans une zone complexe de mélange d’eau minérale, Plaine de Riardo, Sud Italie
Résumé
Les systèmes hydrogéologiques complexes nécessitent une connaissance approfondie de la dynamique des aquifères pour assurer une gestion appropriée et durable des ressources en eaux souterraines. L’aquifère de la plaine de Riardo, dans le Sud de l’Italie, est une ressource stratégique pour des utilisations communes; néanmoins, le modèle conceptuel souffre encore de certaines incertitudes compte tenu de la présence d’arrivée d’eau latérale profonde à travers le substratum carbonaté. Par conséquent, la réalisation d’un modèle numérique 3D à l’échelle du bassin versant nécessite des tests préliminaires afin de limiter le possible débit d’entrée supplémentaires, qui n’est pour le moment estimé que par les résultats du calcul du bilan des eaux souterraines. FEFLOW a été utilisé pour modéliser une section 2D de la zone de mélange afin de tester l’hypothèse d’une recharge combinée. Sept versions, du même modèle, ont été calibrées sur un nombre croissant de paramètres ajustables en fonction de leur sensibilité. La version du modèle la plus efficace a été identifiée selon les critères d’information calculés et la somme des résidus pondérés au carré. Dans la deuxième phase du travail, neuf scénarios de modèle caractérisés par différents débits d’arrivée profondes ont été calibrés et validés selon la même procédure que le premier modèle, afin d’identifier la gamme de solutions acceptables possibles. Le flux d’eau profonde le plus probable correspond à 34 ± 4% de la recharge totale ce qui correspond à une contribution d’eau profonde estimée à 415 ± 50 L/s à l’aquifère de la plaine de Riardo à travers le substratum carbonaté. Cette approche méthodologique servira de base aux modèles numériques 3D de la plaine de Riardo et peut constituer un outil précieux pour la conceptualisation de zones d’eau minérale similaires.
Modelado bidimensional simplificado para limitar la contribución de agua subterránea profunda en una zona de mezcla compleja de agua mineral, Riardo Plain, Sur de Italia
Resumen
Los sistemas hidrogeológicos complejos requieren un conocimiento detallado de la dinámica de los acuíferos para garantizar una gestión adecuada y sostenible del recurso de aguas subterráneas. El acuífero de Riardo Plain, en el sur de Italia, es un recurso estratégico para usos conjuntivos; sin embargo, el modelo conceptual todavía sufre algunas incertidumbres debido a la presencia de un profundo flujo lateral a través del basamento carbonático. Por lo tanto, la realización de un modelo numérico 3D a escala de captación necesita pruebas preliminares para limitar la posible tasa de entrada adicional, que en este momento solo se estima a través de los resultados del cálculo del balance de aguas subterráneas. Se modeló una sección 2D del área de mezcla utilizando FEFLOW para probar la hipótesis de una recarga combinada. Siete versiones del mismo modelo se calibraron sobre un número creciente de parámetros ajustables de acuerdo con su sensibilidad. La versión del modelo más eficiente se identificó de acuerdo con los criterios de información calculados y la suma de los residuos ponderados al cuadrado. En la segunda fase del trabajo, se calibraron y validaron nueve escenarios de modelos caracterizados por diferentes tasas de entrada profundas de acuerdo con el mismo procedimiento del primer modelo, a fin de identificar el rango de posibles soluciones aceptables. La tasa de entrada profunda más probable es 34 ± 4% de la recarga total, lo que corresponde a una entrada profunda estimada de 415 ± 50 L/s en el acuífero de Riardo Plain a través del basamento carbonático. Este enfoque metodológico será la base de los siguientes modelos numéricos 3D de Riardo Plain y puede ser una herramienta valiosa para conceptualizar áreas similares de agua mineral.
意大利南部里亚尔多平原复杂矿水混合地区促进深部地下水贡献率的简化二维模拟
摘要
复杂水文地质系统需要详细的含水层动力学知识以确保地下水资源的恰当的、可持续的管理。意大利南部里亚尔多平原含水层是综合利用的战略资源;由于存在着通过碳酸盐基岩的深部侧向流入,概念模型仍然遇到一些不确定性。因此,建立流域尺度上的三维数值模型需要促进可能的额外流入量的初步试验,目前这个额外流量只能通过地下水平衡计算结果估计。利用FEFLOW模拟了混合区的二维剖面,以测试联合补给的假设。根据其灵敏度,采用越来越多的可调整参数对七个版本的同一模型进行了校正。根据计算的信息标准以及平方加权残差之和确定了最有效率的模型版本。在工作的第二阶段,根据第一个模型相同的程序,对不同深部流入量的九个模型方案进行了校准和验证,以确定可能可接受方案的范围。最可能深部流入量为总补给的34 ± 4%,与通过碳酸盐基岩的里亚尔多平原含水层估算的深部流入量415 ± 50 L/s一致。该方法是遵循里亚尔多平原数值三维模型的基础,可以成为概念化类似矿物水地区的宝贵工具。
Modelagem bidimensional simplificada para restringir a contribuição profunda das águas subterrâneas em uma área de mistura complexa de água mineral, Planice de Riardo, Sul da Itália
Resumo
Sistemas hidrogeológicos complexos requerem conhecimento detalhado das dinâmicas do aquífero para assegurar o gerenciamento apropriado e sustentável dos recursos hídricos subterrâneos. O aquífero da planice de Riardo, Sul da Itália, é um recurso estratégico para usos conjuntivos; no entanto o modelo conceitual ainda sofre algumas incertezas devido a presença de um influxo lateral profundo através do embasamento de carbonato. Portanto a realização de um modelo numérico 3D na escala de bacia precisa de testes preliminares para restringir possíveis taxas adicionais de influxo, que no momento é apenas estimada pelos resultados do calculo do balanço de água subterrânea. Uma seção 2D da área de mistura foi modelada usando o FEFLOW para testar a hipótese de uma recarga combinada. Sete versões do mesmo modelo foram calibradas em um número crescente de parâmetros ajustáveis de acordo com sua sensibilidade. A versão mais eficiente do modelo foi identificada de acordo com os critérios de informação calculados e a soma dos quadrados dos desvios ponderados. Na segunda fase do trabalho, nove cenários de modelo caracterizados por diferentes taxas de influxo profundo foram calibrados e validados de acordo com o mesmo procedimento do primeiro modelo, a fim de identificar a faixa de possíveis soluções aceitáveis. A taxa de influxo profunda mais provável é de 34 ± 4% da recarga total, correspondendo a um influxo profundo estimado de 415 ± 50 L/s no aquífero da Planice de Riardo através do embasamento de carbonato. Essa abordagem metodológica será a base para futuros modelos numéricos 3D da Planice de Riardo e pode ser uma ferramenta valiosa na conceitualização de áreas similares de água mineral.
Introduction
Numerical modelling of aquifers at catchment scale is a fundamental tool for the management of all groundwater resources, especially in strategic aquifers exploited for conjunctive purposes. In addition, numerical modelling is a powerful tool to test conceptual models in which some budget terms cannot be easily estimated or directly measured as in the case of overlapping aquifers, where the possible range of the contribution of deep aquifers in vertical mixing areas can be only estimated (Baiocchi et al. 2013; Maréchal et al. 2013). The numerical models must be supported by reliable hydrogeological conceptual models (Poeter and Anderson 2005; Singh 2014; Zhou and Herath 2017) in order to define the geometry and hydraulic properties of the aquifer layers and the boundary conditions, which influence the simulated system.
The implementation of a regional threedimensional (3D) numerical model usually suffers many uncertainties depending on the model scale, geometry of the aquifer and reliability of the applied boundary conditions (Bredehoeft 2005; Hill and Tiedeman 2007; Renz et al. 2009; Sepúlveda and Doherty 2015; Giacopetti et al. 2016; Andrés et al. 2017; Lancia et al. 2018). In addition, the calibrated solution is nonunique, as well as dependent on the quantity and quality of observation data and accuracy during field data collection (Poeter and Anderson 2005; Singh et al. 2010).
Many approaches (Hill 2006; Foglia et al. 2007; Singh et al. 2010; Ye et al. 2010) have been proposed to reduce the uncertainty of a model, using simplifications of the structure and/or statistical methods to quantify the uncertainty when its irreducible limit is reached.
Some authors have reduced the amount of information required through the building of twodimensional (2D) models, where the absence of the third dimension limits the number of adjustable parameters (Sena and Molinero 2009; Pola et al. 2015; Lancia et al. 2018). In fact, 2D numerical investigations can be performed isolating the salient hydrogeological properties, to explain specific dynamics, which cannot be understood otherwise, due to the high number of unknowns at regional scale.
One of the present approaches makes use of parsimonious models (Carrera and Neuman 1986a, b, c; Massmann et al. 2006; Hill and Tiedeman 2007). Such an approach requires a limited number of parameters to be estimated, where the ideal number is supported by the content of information present in the data. Parsimonious models rely on this limit, since manual regularisation of parameters is applied (geometry of the parameters homogeneous zones is arbitrarily defined manually according to the conceptual model). In this case, as the number of parameters increases, the dataset content of information becomes insufficient to adjust all of them and uncertainty increases consequently. To overcome this limit, highly parametrised methods have been developed (Doherty 2010; Anderson et al. 2015) that are able to better accommodate the salient complexity of reality; the uniqueness of the solution in this case is achieved through mathematical regularisation (i.e., Tikhonov regularisation in PEST). Unlike manual regularisation that seeks uniqueness through inverse problem reduction, with Tikhonov regularisation prior information is added about the parameter field (an additional “parameter observations” dataset including hydraulic test results and other expert knowledge information), so that even illposed inverse models can be numerically solved (Doherty 2015).
In the case of the parsimonious approach, the model performances can be evaluated through the information criteria (Engelhardt et al. 2014; Giacopetti et al. 2016), which provide information about the quality of the model estimation, considering both the goodness of the calibration and the complexity of the model.
Riardo Plain aquifer is a strategic drinking water resource for more than 100,000 people, the water storage for 60 km^{2} of irrigated land, and the source of a mineralwaterbottling plant. The hydrogeological framework of Riardo Plain has been studied since the 1990s by several research teams but its conceptual model still suffers some uncertainties due to the complexity of the aquifer dynamics. Indeed, two aquifers can be identified in the study area: a multilayered volcanic aquifer and a deep confined carbonate aquifer locally mixing with the above volcanic aquifer. The groundwater budget calculation suggested the presence of an additional source of recharge deriving from the lateral inflow through the carbonate ridges surrounding the plain, driven by the sedimentary basement under the volcanic deposits and locally upflowing in the mineral water mixing area. The recognised complexity of the Riardo Plain hydrogeological setting can be a challenge to test a numerical modelling approach for the validation of the conceptual model and then the management of a complex aquifer, exploited for conjunctive purposes.
With the present level of knowledge, the 3D numerical model of the entire Riardo Plain aquifer suffers due to the high number of unknown parameters, especially a validated additional deep recharge, and due to the clustered distribution of the observations. The first step is, therefore, the validation of the last conceptual model elaborated, focusing on the reliability of the presence of a deep inflow and providing the most efficient range of possible flow rate solutions.
In this study, a simplified approach on a 2D submodel using information criteria constraints was applied. Inapplicability of complex 3D hydrological models due to scarce data motivated the need for the simplified 2D modelling approach in an attempt to constrain the results to the available data, isolating the most relevant system processes. The investigated portion of the aquifer is in close proximity to the mineralwatermixing area, where the volcanic and the carbonate aquifers are still unmixed, and could be separately monitored.
The proposed combined approach has allowed a preliminary 2D evaluation of the additional deep recharge of the aquifer, particularly useful in following thermal and mineralaquifer3Dnumerical simulation, being the deep resource typically with higher economic relevance, but also harder to directly quantify. Indeed, a 3D aquifer model can be affected by high uncertainties in such hydrogeological frameworks, typically concerning flow rate and up flow localisation. The preimplementation of a 2D model of the mixing area could provide insight on the system unknowns.
Geological and hydrogeological framework
The basement corresponds to the MesoCenozoic Apennine carbonate sequences, highly deformed since the Miocene during the orogenetic phase and later during the PlioPleistocene distensive tectonic activity, which displaced the basement via numerous horst and graben (Giordano et al. 1995; Cosentino et al. 2006; Turco et al. 2006; Boncio et al. 2016). The same carbonate units crop out in the mountain ridges (D’Argenio and Pescatore 1962) which surround the volcano edifice and the Riardo Plain (Mount Maggiore, Fig. 1).
The morphology of the carbonate basement under the volcanic deposits was mainly deduced by geophysical investigations (Capuano et al. 1992; Nunziata and Gerecitano 2012), integrated with some published and unpublished borehole data (Watts 1987; Ballini et al. 1989; Giordano et al. 1995, Saroli et al. 2017; Ferrarelle S.p.A., unpublished data, 2015). Most of the available stratigraphic data derive from sites located near Riardo Town, in correspondence with the mineral water plant. Locally, the borehole data reveal a highly deformed basement, which generally deepens from an elevation of about 110 m above sea level (a.s.l.) near the boundaries of the Riardo Plain, to 100 m below sea level (b.s.l.) moving eastward, toward the volcano edifice.
The Riardo Plain was mostly filled by the volcanoclastic and the ignimbrite units from the Roccamonfina Volcano, whose activity started around 550 ka and ended about 150 ka (Rouchon et al. 2008).

Campanian Ignimbrite unit (39 ka): ashy facies, characterised by low primary porosity, of the ignimbrite erupted from the Campi Flegrei volcanic district (De Vivo et al. 2001) after the end of the activity of the Roccamonfina Volcano.

Upper pyroclastic unit (from ca. 350 to ca. 330 ka): alternation of reworked volcanic deposits and pumice–rich ignimbrite unit. The unit shows a good overall primary porosity and lower vertical permeability.

Brown Leucitic Tuff ignimbrite (BLT) unit (ca. 350 ka): lithic tuff in ash matrix, characterised by low primary porosity (Luhr and Giannetti 1987). The unit sometimes shows a vertical fracture pattern. The unit shows variable thickness and features according to the ignimbrite deposition.

Basal volcanoclastic unit: alternation of reworked volcanic deposits with a granular range spanning between ashes and pumices. The unit is characterised by a good overall primary porosity. The presence of layers with different porosity reduces the vertical permeability of the unit.
According to the geological framework, an upper multilayer volcanic aquifer and a deeper carbonate one can be distinguished at the regional scale. The two aquifers are separated by a noncontinuous clay unit (Flysch unit; Capelli et al. 1999). The borehole stratigraphic data, in fact, identified some areas where the volcanic deposits are directly deposited over the carbonate basement. This geological setting is in accordance with the regional geologic reconstruction of the study area (Saroli et al. 2014), in which the clays should be preserved in the graben and, in contrast, eroded on the horst.
The multilayered volcanic aquifer presents a radial flow from the Roccamonfina Volcano towards gaining streams (Savone River, Fig. 1) and is mainly recharged by direct infiltration (Celico 1983; Boni et al. 1986; Viaroli et al. 2016a, b). The boundaries of the hydrogeological basin are mainly defined along the groundwater divides of the volcanic aquifer (Fig. 1), even if the extension of the recharge of the whole aquifer system is not precisely defined because of the presence of the deep inflow. The volcanic aquifer is exploited for conjunctive uses, especially for agricultural purposes, which corresponds almost to 60% of the total groundwater requirements.
Points monitoring the carbonate aquifer are mainly clustered in the Ferrarelle S.p.A. mineral water bottling plant near Riardo Town, where the basement upraises and the fault systems allow local mixing between the carbonate and volcanic aquifers (Cuoco et al. 2010). As a result, the potentiometric levels of the two aquifers near the mixing area are very similar in absolute values and trends, related to the local seasonal thermo–pluviometric conditions.
The volcanic aquifer shows a low mineralisation (electrical conductivity (EC) around 350 μS/cm) and HCO_{3}Na, K water type, with a moderate amount of dissolved carbon dioxide (around 200 mg/L; Cuoco et al. 2010, 2015). The mean hydraulic head, measured under static conditions in all wells tapping this aquifer layer, was around 112 m a.s.l.
The high mineralised carbonate aquifer (EC around 3,100 μS/cm) shows HCO_{3}Ca water type, relatively enriched in volcanic ions (F^{−}, K^{+}, As, Fe) and a high CO_{2} content (around 1,900 mg/L). This aquifer shows a mean hydraulic head around 112 m a.s.l. with annual cycles as well.
Groundwater budget, calculated on the recharge area of the Riardo Plain aquifer in the 1992–2014 period, showed a significant water deficit (average 485 L/s/year), without providing any evidence of aquifer overexploitation. In fact, in face of the calculated water deficit, the hydraulic head monitoring in the same period showed almost stable values. This result suggested the presence of an external inflow through the carbonate aquifer, probably recharged by the carbonate ridges surrounding the Riardo Plain. Direct calculation of the external recharge rate is not feasible, but it was preliminarily assumed similar to the calculated water deficit (Viaroli et al. 2018).
Materials and methods
Available data and information
Hydraulic properties
The hydraulic conductivity and the specific storage of the geological units were estimated by the interpretation of step drawdown tests and aquifer pumping tests realised in wells tapping the volcanic or the carbonate units, when available, or interpreting borehole stratigraphic data.
Timepumping rates and timedrawdown data were processed adopting an inverse approach using the MLU 2.25 software (Hemker and Maas 1987; Hemker and Post 2010). MLU is based on an analytical solution involving Stehfest’s numerical inversion of the Laplace transform and the LevenbergMarquardt algorithm for parameter optimisation (Abdelaziz and Merkel 2012; Sahoo and Jha 2017). MLU assumes a homogenous, isotropic, and uniform aquifer.
Five drawdown tests and three aquifer tests were performed in the last decade over four wells tapping the volcanic nonmineralised aquifer (upper pyroclastic unit; Fig. 2). The elaborations gave similar results in hydraulic conductivity (5 m/d < k > 50 m/d) and storage (5 × 10^{−3} < S > 5 × 10^{−4}), therefore, a mean value of each parameter was associated with the unit.
Pumping test data on wells tapping the basal volcanic units are not available; notwithstanding, the same initial conductivity and storage values were also associated with this zone, taking into account the similarities in the texture feature with the upper pyroclastic unit. Most of the units were considered isotropic except the upper pyroclastic and the basal volcanoclastic units, characterised by lower vertical hydraulic conductivity due to the layered alternation of volcanic deposits with a grain size ranging between ashes and pumices. A 0.1 vertical anisotropy of the conductivity coefficient was applied to these units. The hydraulic parameters of the carbonate basement were calculated from five tests conducted over the PzC monitoring well and another two productive wells (Fig. 2) tapping the mineralised carbonate aquifer.
Head observations
The hydraulic head observations come from the Ferrarelle S.p.A. database on the monitoring and productive wells placed in the mineral water claim area. Two monitoring wells (PzV and PzC) located along the 2D model section were chosen as significant for the dynamics of the volcanic and carbonate portions.
Numerical methods and processing
The 2D finite element numerical model was implemented using the FEFLOW code (Trefry and Muffels 2007), which applied the finite element approach to the calculation of the flow, mass and heat transport simulations. The numerical model was calibrated via inverse modelling through FePEST (graphical user interface of the PEST code; Doherty 2010).
Calibration over the hydraulic conductivity zones was preliminarily performed under steady–state conditions, using the mean hydraulic head values for the PzC and PzV observation points. The mean zenithal recharge value was applied as Neumann BC. The parameter ranges for the zones defined by pumping tests were set as ± one order of magnitude of the initial value of hydraulic conductivity. A wider range defined by reliable parameter values was associated to the other zones. The steadystate calibration results were used to perform the transient calibration, applying the same bounds of calibration for the hydraulic conductivity and adding the storage as a parameter to be estimated. The model was calibrated according to 24 mean monthly hydraulic head values measured in PzC and PzV during 2003.
Along with the calibration process, sensitivity analysis was performed. Ranking the parameters according to their sensitivity, simpler versions of the model were calibrated selecting different numbers of parameters with higher sensitivities. After the calibration, the models were validated over the 2000–2014 interval, according to about 360 hydraulic head observations. Residuals, observation sensitivities and information criteria were calculated for each calibration run. Comparison among the different results allowed the ranking of versions of the model drawing more information based on the available data, without overfitting the observations, in accordance with the principle of parsimony.
This principle attests that as the number of parameters increases in a model, the calibration improves, but not the model reliability because the model starts to reproduce not only the behaviour of the physical system, but also the noise associated with the data. Therefore, there should be a balance between the quantity of data and the number of parameters that can be calibrated, as expressed by the information criteria.
In a first version of the model, the deep inflow was set according to the preliminary conceptual model described in Viaroli et al. (2018). Another eight versions of the model with different bottom inflow were implemented and calibrated following the same procedure, in order to define the sensitivity of the deep inflow and to define a possible range for this fundamental unknown.
The bottom recharge was kept constant along the simulation period, since it was assumed that time variability of deep circuits is negligible with respect to the direct infiltration. The direct infiltration was applied on a monthly basis according to the budget time series. Therefore, the conceptual model tested was that the wavelength, frequency and trend of hydraulic head oscillations are only a function of the volcanic aquifer, which is directly affected by the zenithal recharge, while the absolute average head value (m a.s.l.) is given by the combination of the direct infiltration and the deep inflow through the carbonate basement.
Highly parametrised methods associated with NullSpace Monte Carlo (NSMC) analysis applied to the groundwater modelling (Tonkin and Doherty 2009; Herckenrath et al. 2011; Anderson et al. 2015; Alberti et al. 2018) could provide better insights about the uncertainty associated with the model predictions, enabling the model to fit the observed data with a stochastic distribution of parameters. Nevertheless, given the limited extension of the 2D model domain, its simplified and relatively known geometry, and its vertical dimension, the classical manual regularisation of parameters was performed through hydraulic conductivity zones definition. Without mathematical regularisation used in the highly parametrised approach, NSMC is not applicable.
Model complexity definition using information criteria
Hydrologic environments are complex systems that can be described by numerical simulators, but with difficulty. Multiple interpretations and mathematical descriptions can exist for the same context, regardless of the quantity and quality of available data. Different hydrogeological models can focus on different aspects of a system, isolating or neglecting the aspects which are not relevant to the aim of the numerical model. If the illusion of the “perfect simulator” is nevertheless pursued, models can suffer the nonuniqueness of the numerical solution. The best way to control this limit is to apply the mathematical regularisation to the spatial distribution of the parameters, entering the domain of the highly parametrised approach. In cases where the geology is well defined and the model structure is kept relatively simple, a parsimonious model can be built in an attempt to provide good model performances with as few calibrated parameters as possible (Engelhardt et al. 2014). There are different approaches to define the better compromise between a good model performance and a limited number of calibrated parameters (Massmann et al. 2006; Hill and Tiedeman 2007; Engelhardt et al. 2014). One of these approaches is based on the definition of the information criteria such as Akaike information criterion (AIC; Akaike 1973), the Bayesian information criterion (BIC; Schwarz 1978) and Kashyap’s information criterion (KIC; Kashyap 1982). These criteria discriminate between models based on how closely they reproduce hydrologic observations (favouring models that reproduce observed behaviour most closely) and how many parameters they contain (penalising models that contain too many; Ye et al. 2010). The criteria applied herein are reported in the following.
Akaike’s information criterion (AIC)
Bayesian information criterion (BIC)
Kashyap’s information criterion (KIC)
Model performance evaluation

The root mean square error (RMSE) provides a quantitative measure of the model error expressed in the units of the variable. When it is equal to 0, it indicates a perfect correspondence between observed and simulated values; the increase in RMSE values indicates an increasingly poor correspondence.
where n corresponds to the number of the observations, P_{i} the ith simulated value and O_{i} the ith observed value.$$ \mathrm{RMSE}=\sqrt{\frac{\sum_{i=1}^n{\left({P}_i{O}_i\right)}^2}{n}} $$(6) 
The NashSutcliffe Model Efficiency (NSE; Nash and Sutcliffe 1970) considers the ratio of the model error to the variability of the data. NashSutcliffe efficiencies can range between −∞ and 1. Values between 0 and 1 are generally viewed as acceptable levels of performance, whereas values less than 0 indicate unacceptable performance. An efficiency of 1 corresponds to a perfect match between model and observations, whereas a value close to zero indicates that the model predicts individual observations no better than the average of the observations. Nevertheless, NSE values higher than 0.65 denote an excellent match (Adamowski and Chan 2011; Golmohammadi et al. 2014; Matiatos et al. 2014).
where n corresponds to the number of the observations, P_{i} the ith simulated value and O_{i} the ith observed value. \( \overline{O} \) corresponds to the mean observed data.$$ \mathrm{NSE}=1\frac{\sum_{i=1}^n{\left({O}_i{P}_i\right)}^2}{\sum_{i=1}^n{\left({O}_i\overline{O}\right)}^2} $$(7) 
Pearson correlation coefficient (R) indicates the strength and direction of a linear relationship between two variables (in this study, observed and simulated values). The correlation is +1 in the case of a perfect increasing linear relationship and − 1 in the case of a decreasing linear relationship. The values in between indicate an intermediate correlation degree, a value higher than 0.7 denotes a significant correlation (Tichy 1993):
where n corresponds to the number of the observations, P_{i} the ith simulated value and O_{i} the ith observed value. \( \overline{O} \) corresponds to the mean observed data and \( \overline{P} \) corresponds to the mean simulated value.$$ R=\frac{\sum_{i=1}^n{\left({O}_i\overline{O}\right)}^2{\left({P}_i\overline{P}\right)}^2}{\sqrt{\sum_{i=1}^n{\left({O}_i\overline{O}\right)}^2}\sqrt{\sum_{i=1}^n{\left({P}_i\overline{P}\right)}^2}} $$(8) 
The RMSEobservations standard deviation ratio (RSR) corresponds to the ratio of the RMSE and standard deviation of measured data. RSR varies from the optimal value of 0, to a large positive value. The lower RSR depends on good model simulation performance and therefore on low RMSE value. The ratio is expressed as follows:
where n corresponds to the number of the observations, P_{i} the ith simulated value and O_{i} the ith observed value. \( \overline{O} \) corresponds to the mean observed data.$$ \mathrm{RSR}=\frac{\mathrm{RMSE}}{{\mathrm{SD}}_{\mathrm{obs}}}=\left[\frac{\sum_{i=1}^n{\left({O}_i{P}_i\right)}^2}{\sqrt{\sum_{i=1}^n{\left({O}_i\overline{O}\right)}^2}}\right] $$(9) 
When the average of residuals is far from zero, the residuals present a bias. The bias can be normalised (NBI) to quantify the relative departure from simulated and observed values:
where \( \overline{P} \) corresponds to the mean simulated value and \( \overline{O} \) corresponds to the mean observed data.$$ \mathrm{NBI}=\frac{\left(\overline{P}\overline{O}\right)}{\overline{O}} $$(10)
The aforementioned statistical descriptors of the residuals were calculated for all the different versions of the model (nine model scenarios with different deep inflow rates). The comparison of the results allowed the definition of a range of more reliable results in the deep inflow estimation.
Postcalibration matrices
At the end of the elaborations on the validation model, PEST provides three matrices: the postcalibration parameter covariance matrix, the parameter correlation coefficient matrix, and the matrix of eigenvectors of the parameter covariance matrix (the latter two matrices being derived from the first).
The uncertainties calculated in this way take no account of the manual regularisation that is normally required to formulate a wellposed inverse problem. The covariance matrix is always a square symmetric matrix with as many rows (and columns) as the adjustable parameters. The variances and covariances reported in the covariance matrix are valid only if the linearity assumption upon which their calculation is based is valid. The diagonal elements of the covariance matrix are the postcalibration variances of adjustable parameters. The offdiagonal elements of the covariance matrix represent the covariances between parameter pairs.
As is pointed out by Doherty (2015), while the information contained in the correlation coefficient matrix has the potential to inform whether the inverse problem is currently illposed (or is approaching this condition), and whether excessive parameter correlation is responsible for this condition, in practice, values calculated for elements of this matrix can often be deleteriously affected by the very illposedness that they seek to expose.
The eigenvalues and eigenvectors of the postcalibration covariance matrix are a far more reliable source of information in this regard.
The eigenvector matrix is composed of as many columns as there are adjustable parameters, each column containing a normalised eigenvector of the postcalibration covariance matrix. Because a covariance matrix is positivedefinite, these eigenvectors are real and orthogonal; they represent the directions of the axes of the postcalibration probability “ellipsoid” in the mdimensional space occupied by the madjustable parameters. The square root of each eigenvalue is the length of the corresponding semi axis of the postcalibration probability ellipsoid in mdimensional adjustable parameter space. If the ratio of a particular eigenvalue to the lowest eigenvalue of the postcalibration covariance matrix is particularly large, then the respective eigenvector defines a direction of relative insensitivity in parameter space. The eigenvector pertaining to the highest eigenvalue is particularly worthy of attention in many parameter estimation problems, for this defines the direction of maximum insensitivity, and is hence of greatest elongation of the postcalibration probability ellipsoid in adjustable parameter space. The ratio (called condition number; Carrera and Neuman 1986a) of the highest to lowest eigenvalue of the postcalibration covariance matrix is of particular importance. If it is too high, then inversion of this matrix becomes numerically difficult (leading to a spurious inverse matrix), or even impossible. In the parameter estimation context, this is an outcome of the fact that solution of the inverse problem approaches nonuniqueness as elongation of the postcalibration parameter probability ellipsoid increases to infinity.
Model building
Model mesh and properties
The 2D model focuses on a small but significant section located west of the Ferrarelle S.p.A. mineral bottling plant where it is possible to understand the dynamics, which regulates the aquifer of the Riardo Plain that sources the mineral water. The model section is located in the unique area (Fig. 1) where it is possible to separately distinguish and monitor the volcanic and carbonate aquifer. The carbonate aquifer, covered by the volcanic units, is elsewhere too deep to be exploited or monitored. Furthermore, moving westward, where the carbonate basement upraises due to the tectonic settings, the aquifer dynamics depend on the mixing of the two aquifer layers (Fig. 2).
The model mesh is defined by 4,990 square elements (10 m × 10 m). The vertical slice is around 1,500 m length and 300 m deep (from around 140 m a.sl. to around −160 m a.s.l.), according to the PzC stratigraphic log. The top of the slice was set as horizontal since no significant variations in the ground elevation are present along the section, if compared to its total thickness.

L1 zone corresponds to the detrital and alluvial deposits, with grain sizes ranging between clays to sands, and has a mean thickness of around 10 m

L2 zone corresponds to the Campanian Ignimbrite unit and has a mean thickness of around 10 m

Pt zone corresponds to the upper pyroclastic unit with a mean thickness of around 60 m

BLT zone corresponds to the mean thickness (around 40 m) of the BLT unit in the central and western section of the model

BLT_dx zone corresponds to the eastern portion of the BLT unit, which locally covers the carbonate basement; it appears highly fractured then more permeable

Pi zone corresponds to the basal volcanoclastic unit; it shows a variable thickness from around 100 m up to 0 m moving eastward, due to the upraise of the carbonate basement

Clay zone corresponds to 20 m clay unit which covers the carbonate units in the western sector of the plain and is interrupted in the eastern sector where the carbonate basement upraises

Carb zone corresponds to the limestone units; its geometry is provided by borehole data

F1 zone and F2 zone represent two portions of the “Carb zone” reproducing fault areas and is located at the edge of the basement steps and are expected to present a higher hydraulic conductivity

BC zone corresponds to the eastern column of the model and does not have a physical meaning as it was only used to allow the positioning of the Dirichlet boundary condition at a short distance, even if the real outflow of the system is much farther, maintaining the small dimensions of the model domain; its role can be considered similar to the conductance defined in the General Head Boundary condition in MODFLOW
Initial values of hydraulic conductivity and storage
Model zone  Hydraulic conductivity (m/d)  Hydraulic conductivity (m/s)  Specific storage  Vertical anisotropy of conductivity 

L1 zone  0.0864  1 × 10^{−6}  1 × 10^{−4}  1 
L2 zone  0.0864  1 × 10^{−6}  1 × 10^{−4}  1 
Pt zone  30^{a}  3.5 × 10^{−4}^{a}  1 × 10^{−4}^{a}  0.1 
BLT zone  0.0864  1 × 10^{−6}  1 × 10^{−4}  1 
BLT_dx zone  20  2.3 × 10^{−4}  1 × 10^{−4}  1 
Pi zone  30^{a}  3.5 × 10^{−4}^{a}  1 × 10^{−4}^{a}  0.1 
Clay zone  0.000864  1 × 10^{−8}  1 × 10^{−4}  1 
Carb zone  17^{a}  2 × 10^{−4}^{a}  1 × 10^{−7}^{a}  1 
F1 zone  100  1.1 × 10^{−3}  1 × 10^{−4}  1 
F2 zone  100  1.1 × 10^{−3}  1 × 10^{−4}  1 
BC zone  0.008  1 × 10^{−7}  1 × 10^{−4}  1 
Boundary conditions
Input
The direct recharge of the volcanic aquifer was calculated by Viaroli et al. (2018) elaborating the daily thermopluviometric data from eight meteorological stations (Regione Campania, unpublished data, 2015; Ferrarelle S.p.A., unpublished data, 2015) during the 2000–2014 period. Two meteorological stations are placed within the Riardo Plain hydrogeological basin, in correspondence of the Roccamonfina Town and the Ferrarelle S.p.A. mineral water bottling plant (Fig. 1). The other six stations (Cellole, Grazzanise, Pontelatone, Presenzano, Rocca d’Evandro and Sessa Aurunca) are placed around the study basin and cover an area of approximately 900 km^{2}. The rainfall data show a wide variability during the study period, with mean annual values ranging between 580 mm in 2000 and 1,600 mm in 2009.
The monthly actual evapotranspiration, the water surplus and the water deficit calculated by the Thornthwaite’s method (Thornthwaite and Mather 1955), highlight similar climatic trends in all weather stations. The mean recharge period was generally identified from November to April. Considering the existing correlation of the weather variables with the ground elevation, cokriging was applied to spatialize the data over the studied basin using GIS.
The effective infiltration, corresponding to the evaluable recharge, was calculated as percentage of the water surplus, taking into account both the permeability of the hydrogeological complexes outcropping in the basin and the slope of the ground surface. In the study area, the effective infiltration was estimated at 55% of the water surplus, according to Viaroli et al. (2018).
The recharge of the carbonate aquifer, still difficult to evaluate, is likely to upflow from the deep reservoir, according to the hydrogeological conceptual model (Viaroli et al. 2018) under numerical validation in this work. The bottom recharge was applied as a constant value using the Neumann boundary condition applied to the nodes of the lower nodes of the mesh, falling within the carb zone (Fig. 6). Different inflow rates are then tested in another eight model scenarios, with an increasing/decreasing percentage of the original tested inflow. The reliability and efficiency of the simulated deep inflow rate and its constancy during the simulated period are evaluated using statistical indexes.
Output
A Dirichlet boundary condition of 109 m a.s.l. was applied to the eastern boundary column of the model, according to the lower hydraulic head value measured in PzV and PzC (Figs. 3 and 4). No inflow is allowed from the applied boundary condition through the addition of a constrain.
Most of the groundwater withdrawals in the study area are for irrigation purposes. No detailed information about the quantification and the time interval of the agricultural withdrawals is available because the majority of irrigation was carried out using private wells without any official information. The agricultural withdrawals were evaluated in the 2000–2014 period according to local climatic conditions elaborated at monthly scale by Thorntwaithe’s method and the land use information (Viaroli et al. 2018). The presence of water deficit was detected every year in July and August; it implies the absence of available water in the soil, and the evapotranspiration exceeding the rainfall amount. Thus, the plantations are likely to be irrigated to avoid the plant exsiccation. The groundwater required for the plant growth was set equal to the water deficit. This method allows only an estimation of the agricultural withdrawals due to the absence of an official dataset; therefore, exceeding or minor extractions could not be estimated.
In the 2D model, the effect of the agricultural withdrawals was recreated using the well boundary condition (well BC) uniformly scattered on the portion of the volcanic aquifer exploited by most of the agricultural wells. The estimated monthly withdrawal, calculated as the water deficit over the model area, was divided and applied on the 1,056 nodes of the Pt zone (Fig. 6).
Even if the calculated water deficit occurred in July and August, the irrigation period usually occurs from June to September according to the regional directive of groundwater use. The assumed agricultural requirements were then spread over a wider period.
Modelling process results
The bottom recharge was applied according to the conceptual model proposed in Viaroli et al. (2018), i.e. –0.0004 m/d, which corresponds to around 480 L/s. The calibrated hydraulic conductivities approached the order of magnitude determined by the pumping tests, used as prior information.
Values of the calibrated parameters in the optimal version of the MOD1
Zone  Hydraulic conductivity (m/d)  Specific storage 

L1 zone  0.11  1.2 × 10^{−4} 
L2 zone  0.015  7 × 10^{−5} 
Pt zone  48  5 × 10^{−4} 
BLT zone  0.09  2.5 × 10^{−5} 
Pi zone  5  5.7 × 10^{−5} 
Clay zone  1.9 × 10^{−5}  2.6 × 10^{−5} 
Carb zone  90  1 × 10^{−7} 
F1 zone  186  6.6 × 10^{−5} 
F2 zone  200  4.6 × 10^{−5} 
BLT_dx zone  50  4 × 10^{−5} 
BC zone  0.01  8.7 × 10^{−5} 
Statistics on residuals of the optimised version of MOD1
Dataset  RMSE  R  NSE  RSR  NBI 

Complete dataset  0.51  0.77  0.60  0.64  0.001 
Well PzV  0.51  0.79  0.52  0.72  0.0 
Well PzC  0.5  0.78  0.66  0.59  0.0006 
The statistics of the results reported in Table 3 show a good model performance (NSE = 0.6), correlation (R = 0.77) and a small root mean square error (RMSE = 0.51). In addition, the model in 14 years of simulation does not show any bias (NBI ~ 0). Focusing on the statistics of each monitoring well, the results are comparable confirming a good simulation of both the volcanic and the carbonate hydraulic head values.
Groundwater budget simulated over the 2000–2014 period (around 5000 days)
Water budget feature  Inflow (m^{3})  Outflow (m^{3}) 

Neumann BC (total recharge)  8,573  0 
Direct recharge  5,328  – 
Deep inflow  3,245  – 
Dirichlet BC  0  3,739 
Well BC  0  5,184 
Storage  Release: 6,680  Capture: 6,330 
Total  15,253  15,253 
Groundwater inflows and outflows are in balance. The differences in storage are minimal according to the longterm simulation. The term of simulated recharge via Neumann BC corresponds both to the portion of water infiltrated by zenithal recharge and to the deep inflow contribution. By means of a zonal budget calculation, it is possible to distinguish the quantity of water that can be attributed to each of the two recharges (Table 4).
The zonal budget results highlight the amount of deep inflow, which corresponds to around 38% of the total recharge.
Value assigned to each cell simulating the deep inflow (fluid flux BC)
Model scenario  Fluid flux BC (m/d)  Δ Inflow 

MOD2  0  −100% 
MOD3  −0.00016  −60% 
MOD4  −0.00028  −30% 
MOD5  −0.00034  −15% 
MOD1  −0.0004  0 
MOD6  −0.00046  +15% 
MOD7  −0.00052  +30% 
MOD8  −0.00064  +60% 
MOD9  −0.004  +1000% 
Statistics on the residuals of the best simulation of each model version
Model scenario  No. of adjustable parameters  RMSE  R  NSE  RSR  NBI 

MOD2  19  0.55  0.8  0.52  0.70  0.001 
MOD3  19  0.60  0.73  0.45  0.75  0.001 
MOD4  16  0.49  0.75  0.63  0.62  0.001 
MOD5  16  0.45  0.84  0.69  0.57  0.000 
MOD1  22  0.51  0.77  0.60  0.64  0.001 
MOD6  16  0.57  0.7  0.49  0.72  0.001 
MOD7  19  0.63  0.66  0.38  0.80  0.001 
MOD8  19  0.68  0.64  0.29  0.85  0.002 
MOD9  10  0.73  0.4  0.17  0.92  0.000 
Total and deep inflow calculated over the nine model scenarios in the 2000–2014 simulation period (around 5,000 days)
Model scenario  Neumann BC (m/d)  Total inflow (m^{3})  Deep inflow (m^{3})  Deep inflow (%) 

MOD2  0  5,328  0  0 
MOD3  −0.00016  6,617  1,289  19 
MOD4  −0.00028  7,584  2,256  30 
MOD5  −0.00034  8,068  2,740  34 
MOD1  −0.0004  8,573  3,245  38 
MOD6  −0.00046  9,035  3,707  41 
MOD7  −0.00052  9,518  4,190  44 
MOD8  −0.00064  10,486  5,158  49 
MOD9  −0.004  37,566  32,238  86 
Discussion
The double recharge of the Riardo Plain aquifer, hypothesised according to the groundwater budget calculations (Viaroli et al. 2018), was tested using a 2D model in an attempt to constrain the possible ranges of inflows in the studied system. The contribution of an external deep inflow through the carbonate basement was preliminarily assumed equal to the calculated groundwater deficit (around 40% of the zenithal recharge). The Neumann BC, applied to the first model scenario (MOD1), simulated the deep contribution suggested in the conceptual model. The results of the MOD1 calibration and validation are coherent with the proposed conceptual model, based on a longterm groundwater budget calculation. Besides the quantitative results of the budget, another aspect was inspected. The tested hypothesis was that the wavelength and frequency of head oscillations are only a function of the volcanic aquifer behaviour (which includes infiltration and withdrawals), excluding any presence of a detectable modulation (or trend) provided by the deep inflow. At the same time, it was assumed that the absolute average head value (m a.s.l.) was given by the combination of the two inflows.
The statistics on the residuals highlighted a small mean error and a good efficiency index, both for the volcanic and the carbonate portion of the aquifer (Table 3). The a priori assignation of the deep inflow value can give rise to uncertainty due to the lack of an experimental measurement or to the intrinsic uncertainties related to the methods of the estimation of the groundwater budget terms. In the last phase of this work, eight additional model scenarios with different deep inflow rates were calibrated and validated (Table 5). Values of the inflow rates were assigned on the basis of the conceptual model, considering the reliable ranges in agreement with the water budget. The zenithal recharge time series was kept the same in all model versions.
The calibrations of the eight model scenarios reached acceptable results in term of residuals, but in some cases the values of the estimated parameters deviated from the reliable ranges. The MOD2 version, for example, reproduces a model scenario where the recharge contribution derives only from the direct infiltration. This example was introduced simply as an extreme scenario, which has no relationship with the hydrogeological and geochemical data available in the literature (Capelli et al. 1999; Cuoco et al. 2010); therefore, the MOD2 version was neglected despite the acceptable numerical results.
On the opposite extreme, the MOD9 version is characterised by the highest simulated deep inflow (Table 5). The high amount of recharge forced the calibration to move the hydraulic parameters to reach their upper bounds imposed by the assigned ranges. This undesirable condition also reflects the scarce efficiency of the simulation (NSE = 0.15; Table 6).
The postcalibration covariance matrix (recorded when manual regularisation is applied) reports variances and covariances of parameter error (given by the difference between estimated and expected value of parameters). The aim is to obtain variances and covariances as small as possible, reducing uncertainty with respect to the precalibration parameter uncertainty.
Results of MOD5 (calibrated according to 16 adjustable parameters) are reported in the electronic supplemental material (ESM). In general, the covariance matrix values are quite low, even if a few parameters are affected by a high covariance, and the specific storage of the BLT_dx zone (S  blt_dx in the ESM) presents an extremely high variance. This probably means that the calibration dataset contains a low amount of information able to reduce the uncertainty of that parameter.
The correlation matrix shows a wide range of positive and negative correlation values between the parameters involved in the calibration. Sometimes the values are close to the autocorrelation (Hill and Tiedeman 2007); therefore, a deep analysis of the eigenvectors and the eigenvalues (all tables in ESM) is necessary as suggested by Doherty (2015).
The eigenvalues of the 16 eigenvectors of the parameter covariance matrix range between 1.04 × 10^{−4} and 2426. The ratio of the highest to lowest eigenvalue of the postcalibration parameter error covariance matrix is 2.33 × 10^{−7}, which turns out to be lower than 5 × 10^{7}, allowing one to say that the numerical integrity of the inversion process is sufficiently good according to Doherty (2015). Refinement of the manual regularisation strategy could have lowered the ratio value, but the present configuration seemed to represent an acceptable compromise.
All MOD versions reveal a similar information content regarding the deep groundwater inflow. The absence of a significant bias of the simulated data over 15 years confirms the constant or quasiconstant rate of the inflow as already supposed in the hydrogeological conceptual model. Limited changes in inflow rates cannot nevertheless be excluded, nor possible changes over a much longer period with respect to the simulated one.
The most likely deep inflow rate, as suggested by the presented modelling process, is 34% ± 4% of the total recharge. This qualitative range, applied to the quantitative groundwater budget calculations of the Riardo Plain aquifer reported in Viaroli et al. (2018), reveals an estimated inflow of around 415 L/s ± 50 L/s. This amount is in agreement with the hypothesis based only on the analytical groundwater budget calculations. The output variability revealed by the different model scenarios seems to be close to the order of magnitude of the intrinsic and ineliminable errors of the groundwater budget.
Conclusions
The knowledge of the dynamics of an aquifer could be increased using numerical models. This feature is extremely useful when vertical or lateral groundwater exchanges occur without the possibility of direct infield measurements. The presence of external groundwater exchanges could sometimes be supposed only by means of the results of groundwater budget calculations, like in the Riardo Plain aquifer. Geochemical and isotopic data, in fact, are often not able to provide a unique hypothesis on the groundwater circulation in such complex systems. Different conceptual models must be supported by the most widespread number of analyses (hydrogeological, geochemical, etc.) and then tested via numerical simulations.
The implementation of a 3D numerical model at catchment scale could be a significant support for stakeholders and decision makers dealing with aqueducts, mineral water bottling activities and irrigation consortia for sustainable groundwater management. The presence of an additional source of recharge is surely a precious resource, but unfortunately it increases the uncertainties of any model attempt due to the absence of reliable information on the spatial distribution and inflow rate. For this reason, before creating the regional 3D model, the implementation of the small 2D model supported by a wellknown geology and longterm hydraulic head observations, was the first step of the modelling process aimed at providing constraints for the next 3D model phase.
A 2D numerical model of the mixing area in the Riardo Plain was implemented in this study firstly to validate the conceptual model based on the result of the groundwater budget calculation. The simplified 2D model structure allowed the limitation of the unknowns affecting the simulated system, focusing only on the quantification of the inflow percentage through the carbonate basement. Seven versions of the model with an increasing number of adjustable parameters, ranked according to their sensitivities, were calibrated on the hydraulic head observations recorded in 2003 and were then validated over 15 years of monitoring. The comparison of the seven calibrated versions allowed one to identify the more efficient model version using the information criteria in order to further reduce the ranges of results. Once the conceptual model was validated, another eight model scenarios were implemented testing different inflow rates, using the same procedure previously described. The statistical results of the most efficient version of each model scenario allowed one to define a reliable range of inflow rate as 34% ± 4% of the total recharge, if the presently available conceptual model is considered valid. This qualitative range, if applied to the quantitative groundwater budget calculations of the Riardo Plain aquifer, reveals an estimated inflow of around 415 L/s ± 50 L/s.
The percentages of inflow tested through this method will be used as starting conditions in the following 3D modelling at catchment scale, reducing the prior uncertainties of the hydrogeological system and limiting the possible solutions compared to a priori inflow value. The described procedure could easily be applied to similar hydrogeological contexts, helping the step by step understanding of the dynamics of complex aquifers in order to produce more reliable 3D numerical models.
Notes
Acknowledgements
The authors thank the Kataclima team for their support during the modelling sessions. The authors also thank the editor Prof J.M. Lemieux, the associate editor Prof G. Porta, the anonymous reviewer, and Dott. M. Lancia for their helpful suggestions for improving the quality of the manuscript. This work was supported by Ferrarelle S.p.A. funding to the research project of the Roma Tre University on the Roccamonfina Volcano aquifer (research supervisor: Prof. Roberto Mazza).
Supplementary material
References
 Abdelaziz R, Merkel BJ (2012) Analytical and numerical modeling of flow in a fractured gneiss aquifer. J Water Resour Protect 4:657–662. https://doi.org/10.4236/jwarp.2012.48076 CrossRefGoogle Scholar
 Adamowski J, Chan HF (2011) A wavelet neural network conjunction model for groundwater level forecasting. J Hydrol 407(1–4):28–40. https://doi.org/10.1016/j.jhydrol.2011.06.013 CrossRefGoogle Scholar
 Akaike H (1973). Information theory as an extension of the maximum likelihood principle. In: Petrov BN, Csaki F (eds) Second international symposium on information theory. Akademiai Kiado, Budapest, pp 267–281Google Scholar
 Alberti L, Colombo L, Formentin G (2018) Nullspace Monte Carlo particle tracking to assess groundwater PCE (Tetrachloroethene) diffuse pollution in northeastern Milan functional urban area. Sci Total Environ 621:326–339. https://doi.org/10.1016/j.scitotenv.2017.11.253 CrossRefGoogle Scholar
 Anderson MP, Woessner WW, Hunt RJ (2015) Applied groundwater modeling: simulation of flow and advective transport. Academic, San Diego, 630 ppGoogle Scholar
 Andrés C, Ordóñez A, Álvarez R (2017) Hydraulic and thermal modelling of an underground mining reservoir. Mine Water Environ 36:24–33. https://doi.org/10.1007/s1023001503651 CrossRefGoogle Scholar
 Baiocchi A, Lotti F, Piscopo V (2013) Impact of groundwater withdrawals on the interaction of multilayered aquifers in the Viterbo geothermal area (central Italy). Hydrogeol J 21(6):1339–1353. https://doi.org/10.1007/s1004001310005 CrossRefGoogle Scholar
 Ballini A, Barberi F, Laurenzi MA, Mezzetti F, Villa IM (1989) Nuovi dati sulla stratigrafia del Vulcano di Roccamonfina [New data on the stratigraphy of the volcano of Roccamonfina]. Boll Gruppo Nazionale Vulcanolog 5(2):533–555Google Scholar
 Boncio P, Dichiarante AM, Auciello E, Saroli M, Stoppa F (2016) Normal faulting along the western side of the Matese Mountains: implications for active tectonics in the central Apennines (Italy). J Struct Geol 82:16–36. https://doi.org/10.1016/j.jsg.2015.10.005 CrossRefGoogle Scholar
 Boni C, Bono P, Capelli G (1986) Schema idrogeologico dell’Italia Centrale [Hydrogeological scheme of the central Italy]. Mem Soc Geol It 35(2):991–1012Google Scholar
 Bredehoeft J (2005) The conceptualization model problem: surprise. Hydrogeol J 13(1):37–46. https://doi.org/10.1007/s1004000404305 CrossRefGoogle Scholar
 Capelli G, Mazza R, Trigari A, Catalani F (1999) Le risorse idriche sotterranee strategiche nel distretto vulcanico di Roccamonfina (Campania Nordoccidentale) [Strategic groundwater resources in the Roccamonfina volcanic district (northwest Campana region)]. Quad Geolog Appl 4:23–32Google Scholar
 Capuano P, Continisio R, Gasparini P (1992) Structural setting of a typical alkalipotassic volcano: Roccamonfina, southern Italy. J Volcanol Geotherm Res 53(1–4):355–369. https://doi.org/10.1016/03770273(92)90091Q CrossRefGoogle Scholar
 Carrera J, Neuman SP (1986a) Estimation of aquifer parameters under transient and steadystate conditions: 1. maximum likelihood method incorporating prior information. Water Resour Res 22(2):199–210. https://doi.org/10.1029/WR022i002p00199 CrossRefGoogle Scholar
 Carrera J, Neuman SP (1986b) Estimation of aquifer parameters under transient and steadystate conditions: 2. uniqueness, stability, and solution algorithms. Water Resour Res 22(2):211–227. https://doi.org/10.1029/WR022i002p00211 CrossRefGoogle Scholar
 Carrera J, Neuman SP (1986c) Estimation of aquifer parameters under transient and steadystate conditions: 3. application to synthetic and field data. Water Resour Res 22(2):228–242. https://doi.org/10.1029/WR022i002p00228 CrossRefGoogle Scholar
 Celico P (1983) Idrogeologia dell’Italia CentroMeridionale [Hydrogeology of the central and southern Italy)]. Quad Cass Mezz 4(2)Google Scholar
 Cosentino D, Federici I, Cipollari P, Gliozzi E (2006) Environments and tectonic instability in Central Italy (Garigliano basin) during the late Messinian LagoMare episode: new data from the onshore Mondragone 1 well. Sediment Geol 188–189:297–317. https://doi.org/10.1016/j.sedgeo.2006.03.010 CrossRefGoogle Scholar
 Cuoco E, Darrah TH, Buono G, Verreggia G, De Francesco S, Eymold WK, Tedesco D (2015) Inorganic contaminants from diffuse pollution in shallow groundwater of the Campanian plain (southern Italy): implications for geochemical survey. Environ Monit Assess 187(46). https://doi.org/10.1007/s106610154307y
 Cuoco E, Verrengia G, De Francesco S, Tedesco D (2010) Hydrogeochemistry of Roccamonfina volcano (southern Italy). Environ Earth Sci 61(3):525–538. https://doi.org/10.1007/s1266500903633 CrossRefGoogle Scholar
 D’Argenio B, Pescatore T (1962) Stratigrafia del Mesozoico nel gruppo del Monte Maggiore (Caserta) [Stratigraphy of the Mesozoic units of the Mount Maggiore (Caserta)]. Boll Soc Naturalist Napoli 71:55–61Google Scholar
 De Vivo B, Rolandi G, Gans PB, Calvert A, Bohrson WA, Spera FJ, Belkin HE (2001) New constraints on the pyroclastic eruptive history of the Campanian volcanic plain (Italy). Miner Petrol 73(1–3):47–65, doi: https://doi.org/10.1007/s007100170010
 Doherty J (2010) PEST, modelindependent parameter estimation manual. Watermark, Brisbane, Australia, 279 ppGoogle Scholar
 Doherty J (2012) Addendum to the PEST manual. Watermark, Brisbane, AustraliaGoogle Scholar
 Doherty J (2015) Calibration and uncertainty analysis for complex environmental models. Watermark, Brisbane, Australia, 227 ppGoogle Scholar
 Engelhardt I, De Aguinaga JG, Mikat H, Schüth C, Liedl R (2014) Complexity vs. simplicity: groundwater model ranking using information criteria. Groundwater 52(4):573–583. doi: https://doi.org/10.1111/gwat.12080
 Foglia L, Mehl SW, Hill MC, Perona P, Burlando P (2007) Testing alternative ground water models using crossvalidation and other methods. Groundwater 45(5):627–641. https://doi.org/10.1111/j.17456584.2007.00341.x CrossRefGoogle Scholar
 Giacopetti M, Crestaz E, Materazzi M, Pambianchi G, Posavec K (2016) A multimodel approach using statistical index and information criteria to evaluate adequacy of the model geometry in a fissured carbonate aquifer (Italy). Water 8(7):271. https://doi.org/10.3390/w8070271 CrossRefGoogle Scholar
 Giordano G, Naso G, Scrocca D, Funiciello R, Catalani F (1995) Processi di estensione e circolazione di fluidi a bassa termalità nella Piana di Riardo (Caserta, Appennino centromeridionale) [Extensional processes and low thermal fluid circulation in the Riardo Plain (Caserta, central–southern Apennine)]. Boll Soc Geol Ital 144:361–371Google Scholar
 Golmohammadi G, Prasher S, Madani A, Rudra R (2014) Evaluating three hydrological distributed watershed models: MIKESHE, APEX, SWAT. Hydrology 1(1):20–39. https://doi.org/10.3390/hydrology1010020 CrossRefGoogle Scholar
 Hemker K, Post V (2010) MLU for Windows 2.25: user’s guide. SCRIBD, 30 pp. https://www.scribd.com. Accessed December 2018
 Hemker CJ, Maas C (1987) Unsteady flow to wells in layered and fissured aquifer systems. J Hydrol 90(3–4):231–249. https://doi.org/10.1016/00221694(87)900692 CrossRefGoogle Scholar
 Herckenrath D, Langevin CD, Doherty J (2011) Predictive uncertainty analysis of a saltwater intrusion model using nullspace Monte Carlo. Water Resour Res 47:W05504. https://doi.org/10.1029/2010WR009342 CrossRefGoogle Scholar
 Hill MC (2006) The practical use of simplicity in developing ground water models. Groundwater 44(6):775–781. https://doi.org/10.1111/j.17456584.2006.00227.x CrossRefGoogle Scholar
 Hill MC, Tiedeman CR (2007) Effective groundwater model calibration with analysis of data, sensitivities, predictions, and uncertainty. Wiley, Hoboken, NJ, 455 ppCrossRefGoogle Scholar
 Kashyap RL (1982) Optimal choice of AR and MA parts in autoregressive moving average models. IEEE Trans Pattern Anal Mach Intell 4(2):99–104. https://doi.org/10.1109/TPAMI.1982.4767213 CrossRefGoogle Scholar
 Lancia M, Saroli M, Petitta M (2018) A double scale methodology to investigate flow in karst fractured media via numerical analysis: the Cassino plain case study (central Apennine, Italy). Geofluids 2018:2937105, pp 1–12. https://doi.org/10.1155/2018/2937105
 Locardi E (1988) The origin of the Apenninic arcs. In: Wezel FC (ed) The origin and evolution of arcs. Tectonophysics 146:105–123. https://doi.org/10.1016/00401951(88)900856
 Luhr JF, Giannetti B (1987) The Brown Leucitic tuff of Roccamonfina volcano (Roman region, Italy). Contrib Mineral Petrol 95(4):420–436. https://doi.org/10.1007/BF00402203 CrossRefGoogle Scholar
 Maréchal JC, Dewandel B, Ahmed S, Galeazzi L, Zaidi FK (2006) Combined estimation of specific yield and natural recharge in a semiarid groundwater basin with irrigated agriculture. J Hydrol 329(1–2):281–293. https://doi.org/10.1016/j.jhydrol.2006.02.022 CrossRefGoogle Scholar
 Maréchal JC, Lachassagne P, Ladouche B, Dewandel B, Lanini S, Le Strat P, PeteletGiraud E (2013) Structure and hydrogeochemical functioning of a sparkling natural mineral water system determined using a multidisciplinary approach: a case study from southern France. Hydrogeol J 22(1):47–68. https://doi.org/10.1007/s1004001310731 CrossRefGoogle Scholar
 Massmann C, Birk S, Liedl R, Geyer T (2006) Identification of hydrogeological models: application to tracer test analysis in a karst aquifer, calibration and reliability in groundwater modelling: from uncertainty to decision making. IAHS Publ 304, IAHS, Wallingford, UK, pp 59–64Google Scholar
 Matiatos I, Varouchakis EA, Papadopoulou MP (2014) Statistical sensitivity analysis of multiple groundwater mass transport models. Proceedings of 10th International Hydrogeological Congress of Greece, Thessaloniki, October 2010, pp 447–456Google Scholar
 Nash JE, Sutcliffe JV (1970) River flow forecasting through conceptual models part I: a discussion of principles. J Hydrol 10(3):282–290. https://doi.org/10.1016/00221694(70)902556 CrossRefGoogle Scholar
 Nunziata C, Gerecitano F (2012) V_{s} crustal models of the Roccamonfina volcano and relationship with Neapolitan volcanoes (southern Italy). Int J Earth Sci 101:1371–1383. https://doi.org/10.1007/s0053101107227 CrossRefGoogle Scholar
 Peccerillo A (2005) PlioQuaternary volcanism in Italy. Springer, Berlin, 321 ppGoogle Scholar
 Poeter EP, Anderson D (2005) Multimodel ranking and interference in ground water modeling. Ground Water 43(4):597–605. https://doi.org/10.1111/j.17456584.2005.0061.x CrossRefGoogle Scholar
 Pola M, Fabbri P, Piccinini L, Zampieri D (2015) Conceptual and numerical models of a tectonicallycontrolled geothermal system: a case study of the Euganean geothermal system, northern Italy. Cent Eur Geol 58(1–2):129–151. https://doi.org/10.1556/24.58.2015.12.9 CrossRefGoogle Scholar
 Renz A, Rühaak W, Schätzl P, Diersch HJG (2009) Numerical modeling of geothermal use of mine water: challenges and examples. Mine Water Environ 28:2–14. https://doi.org/10.1007/s1023000800633 CrossRefGoogle Scholar
 Rouchon V, Gillot PY, Quidelleur X, Chiesa S, Floris B (2008) Temporal evolution of the Roccamonfina volcanic complex (Pleistocene), central Italy. J Volcanol Geotherm Res 177:500–514. https://doi.org/10.1016/j.jvolgeores.2008.07.016 CrossRefGoogle Scholar
 Sahoo S, Jha MK (2017) Numerical groundwaterflow modeling to evaluate potential effects of pumping and recharge: implications for sustainable groundwater management in the Mahanadi Delta region, India. Hydrogeol J 25(8):2489–2511. https://doi.org/10.1007/s1004001716104 CrossRefGoogle Scholar
 Saroli M, Lancia M, Albano M, Mondoni G, Moro M, Scarascia Mugnozza G (2014) New geological data on the Cassino intramontane basin, central Apennines, Italy. Rendiconti Lincei 25(2):189–196. https://doi.org/10.1007/s1221001403385 CrossRefGoogle Scholar
 Saroli M, Lancia M, Albano M, Casale A, Giovinco G, Petitta M, Zarlenga F, Dell’Isola M (2017) A hydrogeological conceptual model of the Suio hydrothermal area (central Italy). Hydrogeol J 25(6):1811–1832. https://doi.org/10.1007/s1004001715495 CrossRefGoogle Scholar
 Schwarz G (1978) Estimating the dimension of a model. Ann Stat 6(2):461–464CrossRefGoogle Scholar
 Sena C, Molinero J (2009) Water resources assessment and hydrogeological modelling as a tool for the feasibility study of a closure plan for an open pit mine (La Respina mine, Spain). Mine Water Environ 28:94–101. https://doi.org/10.1007/s1023000900677 CrossRefGoogle Scholar
 Sepúlveda N, Doherty J (2015) Uncertainty analysis of a groundwater flow model in eastcentral Florida. Groundwater 53(3):464–474. https://doi.org/10.1111/gwat.12232 CrossRefGoogle Scholar
 Singh A (2014) Groundwater resources management through the applications of simulation modeling: a review. Sci Total Environ 499:414–423. https://doi.org/10.1016/j.scitotenv.2014.05.048 CrossRefGoogle Scholar
 Singh A, Mishra S, Ruskauff R (2010) Model averaging techniques for quantifying conceptual model uncertainty. Groundwater 48(5):701–715. https://doi.org/10.1111/j.17456584.2009.00642.x CrossRefGoogle Scholar
 Thornthwaite CW, Mather JR (1955) The water balance. Climatology 8(1):104Google Scholar
 Tichy M (1993) Applied methods of structural reliability. Springer, Dordrecht, 403 ppCrossRefGoogle Scholar
 Tonkin M, Doherty J (2009) Calibrationconstrained Monte Carlo analysis of highly parametrized models using subspace techniques. Water Resour Res 45:W00B10. https://doi.org/10.1029/2007WR006678 CrossRefGoogle Scholar
 Trefry MG, Muffels C (2007) FEFLOW: a finiteelement groundwater flow and transportmodeling tool. Groundwater 45(5):525–528. https://doi.org/10.1111/j.17456584.2007.00358.x CrossRefGoogle Scholar
 Turco E, Schettino A, Pierantoni PP, Santarelli G (2006) Chapter 2 the Pleistocene extension of the Campania plain in the framework of the southern Tyrrhenian tectonic evolution: morphotectonic analysis, kinematic model and implications for volcanism. In: De Vivo B (ed) Volcanism in the Campania plain Vesuvius, Campi Flegrei and ignimbrites, vol 9. Elsevier, Amsterdam, pp 27–51Google Scholar
 Viaroli S, Cuoco E, Mazza R, Tedesco D (2016a) Dynamics of natural contamination by aluminum and iron rich colloids in the volcanic aquifers of central Italy. Environ Sci Pollut Res 23:19958–19977. https://doi.org/10.1007/s1135601671988 CrossRefGoogle Scholar
 Viaroli S, Mastrorillo L, Mazza R, Paolucci V (2016b) Hydrostructural setting of Riardo plain: effects on Ferrarelle mineral water type. Acque Sotterranee 5(3):59–68. https://doi.org/10.7343/as2016226 CrossRefGoogle Scholar
 Viaroli S, Mastrorillo L, Lotti F, Paolucci V, Mazza R (2018) The groundwater budget: a tool for preliminary estimation of the hydraulic connection between neighboring aquifers. J Hydrol 556:72–86. https://doi.org/10.1016/j.jhydrol.2017.10.066 CrossRefGoogle Scholar
 Watts MD (1987) Geothermal exploration of the Roccamonfina volcano, Italy. Geothermics 16(5–6):517–528CrossRefGoogle Scholar
 Ye M, Meyer PD, Neuman SP (2008) On model selection criteria in multimodel analysis. Water Resour Res 44(3):W03428. https://doi.org/10.1029/2008WR006803 CrossRefGoogle Scholar
 Ye M, Pohlmann KF, Chapman JB, Pohll GM, Reeves DM (2010) A modelaveraging method for assessing groundwater conceptual model uncertainty. Groundwater 48(5):716–728. https://doi.org/10.1111/j.17456584.2009.00633.x CrossRefGoogle Scholar
 Zhou Y, Herath HMPSD (2017) Evaluation of alternative conceptual models for groundwater modelling. Geosci Front 8:437–443. https://doi.org/10.1016/j.gsf.2016.02.002 CrossRefGoogle Scholar
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