1. Introduction

Drylands represent 40% of the world land areas and are home to about 35% of the world population (FAO, 2011; UN, 2011). They are generally defined as those regions with low, scattered and sporadic precipitations exceeded by a very high evapotranspiration (Joly, 2006; FAO, 2011). As a consequence, available and permanent water reserves in those areas are mainly underground (Joly, 2006).

Historically, local populations living in drylands relied on the surface expression of groundwater (springs) as well as on small, often temporary, streams (UN, 2011). They developed complex hydraulic systems, which enable them to take advantage, as much as possible, of the scarce resources. When springs and surface water were not sufficient or inexistent, survival depended on the possibility to tap groundwater. Among the hydraulic systems that have been developed in the ancient world, filtration galleries are considered as one of the oldest and biggest achievements of human engineering (Motiee et al., 2006) and the knowledge behind their construction as a wonder of human civilizations (Semsar Yazdi and Labbaf Khaneiki, 2017).

A filtration gallery is a traditional water manage-ment system used to provide a reliable supply of water in arid and semi-arid climates (Mostafaeipour, 2010). It consists of an underground and almost horizontal tunnel with vertical shaft wells, which tap and drain groundwater to the earth surface. Part of the tunnel is dug into the aquifer, so the water seeps through the tunnel’s walls, floor and ceiling (collection section). The other part of the tunnel runs over the water table, down to the exit point (transport section). Water flows downward by gravity in order to supply water for domestic purpose and irrigate downslope lands (Fig. 1; Lightfoot, 1996; Motiee et al., 2006; Semsar Yazdi and Labbaf Khaneiki, 2017).

Fig. 1. Illustration of a typical filtration gallery. A. Longitudinal section; B. Cross section; C. Aerial view (modified after English, 1968 and Naghibi et al., 2015).

The extension of the galleries through the aquifer increases the contact area of the tunnel with the water-bearing zone and so the height of the water column in the tunnel. When the tunnel extent is carried out in various directions (side branches), the infiltration area increases and, accordingly, the discharge (Lightfoot, 1996; Semsar Yazdi and Labbaf Khaneiki, 2017). The technology was originated in the ancient Armenian-Persian region, about 600-800 years BC (English, 1968; Beaumont, 1971; Lightfoot, 1996; Motiee et al., 2006; Mostafaeipour, 2010; Semsar Yazdi and Labbaf Khaneiki, 2017). From then on, it was spread to other regions and cultures.

Filtration galleries tap in general into alluvial fan aquifers at the limit between mountains and plains (piedmont aquifers). They rely entirely on passive tapping of the water available by gravity and, consequently, the natural supply of water in a filtration gallery can never exceed groundwater recharge (Lightfoot, 1996). For this reason, filtration galleries represent a sustainable and low-cost water supply system. In many countries, they are nowadays abandoned to the benefit of pumped wells and boreholes (Lightfoot, 1996; Motiee et al., 2006; Mustafa and Qazi, 2007). In North Chile, filtration galleries have been identified in four areas: Azapa, Sibaya, La Calera and Pica (Fig. 2). The latter includes the galleries of the nearby towns of Pica and Matilla, and the locality of Puquio Núñez (Barnes and Fleming, 1991). 

Fig. 2. Location of the study area. A. Location of Chile socavones; B. Topographic and geomorphological profile W-E of Chile at the latitude of the study area; C. Map of Pica area.

Pica is an oasis located in the hyper-arid Atacama Desert, at the foothill of the Andean Cordillera, on the Eastern margin of the Central Depression, a relatively flat basin called Pampa del Tamarugal (Fig. 2). The presence of thermal springs and shallow groundwater allows the cultivation of citrus and other tropical fruits, as well as vineyards in the past (Billinhurst, 1893; Bruggen, 1918; Dingman and Gali, 1965). The filtration galleries of Pica, known as socavones, are used for irrigation. They tap the groundwater of the local shallow aquifer of Pica. The origin of Pica’s groundwater and connection with the regional aquifer of the Pampa del Tamarugal has been the subject of several studies since the 1960s (Dingman and Galli, 1965; Suzuki and Aravena, 1985; Salazar et al., 1998; Grilli et al., 1999; Scheihing et al., 2017). Nevertheless, the hydrogeological processes controlling the recharge and discharge of Pica aquifer are still not fully understood.

Billinghurst (1893) mentioned 13 socavones in his publication “The irrigation of Tarapacá” and the discharge flow associated with each gallery. Bruggën (1918) mentioned 23 socavones and gave a basic description of their geology, groundwater origin, temperature and flow. He drew a basic location map, which was the only one in existence. Further studies used the information produced by Bruggën (1918).

Today, the socavones of Pica area are falling into decay. Most are abandoned while groundwater extraction through wells and boreholes increases, leading to groundwater drawdown and salinization. While they are disappearing from local people memories, their exact location remains unknown and many are even not mentioned in the literature. Because of the development of the towns of Pica and Matilla, problems of subsidence and sinkholes appeared, threatening existing infrastructure. Moreover, they were never the subject of a precise description and study, both physical and historical, ruling out the possibility to understand, preserve, highlight and reuse this water management system.

The purpose of this study is to provide the first complete identification and a description of the Pica area filtration galleries with the objectives of i. Preserving water and geoheritage, ii. Contributing to the hydrogeological knowledge of Pica aquifer, and iii. Improve land-use planning. Such information is required to ensure the environmental and socio-economic sustainability of the oasis of Pica area, in particular regarding groundwater management and the potential subsidence risks resulting from the expansion of Pica and Matilla towns. Based on the underground exploration and mapping, completed by geophysical prospection, the physical, geological and hydrogeological characteristics of the socavones were studied. The findings allow to highlight the originality of the galleries, as geo and water heritage of the Atacama Desert, and to review and complete the hydrogeological conceptual model of Pica aquifer. Although the socavones of Pica are today mostly abandoned, this study gives also an insight of the potential role that the galleries may still play in the groundwater management of the oasis.

2. Methodology

2.1. Study area

Pica is located in the Region of Tarapacá (northern Chile) at about 20°30’ S and 69°20’ W (Fig. 2)    and is part of the Atacama Desert, one of the driest places on earth (Weishet, 1975). The oasis lies at an altitude of 1,500 m a.s.l., in the piedmont area, at the junction between the Precordillera (Altos de Pica) and the Central depression (Pampa del Tamarugal, Fig. 2B and C).

Average annual rainfall is almost null in the Pampa del Tamarugal and less than 10 mm in the Pica area therefore no direct recharge occurs from precipitation in the area (Rojas and Dassargues, 2007; Lictevout et al., 2013; Viguier, 2016). Rainfall increases with altitude, reaching an annual mean of 150-180 mm in the Precordillera, Altiplano and Cordillera, of which 80% occurs between December and March (Houston, 2006; Acosta and Custodio, 2008; DIHA-PUC, 2009; Lictevout et al., 2013). Inter-annual variability is very high, influenced by global phenomenon as El Niño Southern Oscillation (ENSO) and the regional wind patterns (Garreaud and Aceituno, 2001; Montecino and Aceituno, 2003).

Narrow and deep valleys (quebradas) incise the Piedmont from East to West and drain the water from the highlands down to the Central Depression through huge alluvial fans. The Pampa del Tamarugal and Piedmont area consist of sedimentary deposits and pyroclastic flows (ignimbrites) produced by the eruption and erosion of the volcanic arc of the Andean Cordillera from the end of the Oligocene to the modern period (Moreno and Gibbons, 2007). It overlaps with a major discordance the pre-Oligocene volcano-sedimentary, metamorphic and plutonic basement (Lamb et al., 1997; Farías et al., 2005; Hartley and Evenstar, 2010; Jordan et al., 2010, 2014). The Cenozoic cover harbour groundwater reserves recharged in the Precordillera and flowing down through the piedmont area (Rojas and Dassargues, 2007; Jayne et al., 2016; Viguier et al., 2018). The shallow aquifer of Pica is located in the late Cenozoic cover (Pleistocene-Holocene alluvial deposits). A regional structural height (Longacho Flexure, Fig. 3), constituting a natural barrier to the groundwater flows coming from the East, and underlying impermeable layers allow the formation of a shallow aquifer in the Pica basin with the emergence of thermal springs.

 

Fig. 3. Geological map of Pica area (modified after Blanco et al., 2012a and Blanco and Tomlinson, 2013).

Two recharge models have been proposed for the aquifer of Pica: one model (Dingman and Galli, 1965; Fritz et al., 1981; Suzuki and Aravena, 1985; Salazar et al., 1998; Grilli et al., 1999; Rojas et al., 2010; Jayne et al., 2016; Scheihing et al., 2017) considers that recharge takes place in Pica’s head catchment (Altos de Pica), above 3,500 m a.s.l. (Precordillera). The precipitation infiltrates through the Huasco ignimbrites strongly fractured and flows downward through the lower layers of the Altos de Pica Formation (Sagasca Member) which consists of Oligo-Miocene volcano-sedimentary deposits, an alternation of thick continental sedimentary sequences (sandstone and conglomerates) and thinner volcanic horizons (Huasco and Tambillo ignimbrites; Figs. 3 and 4). The Altos de Pica Formation unconformably overlies the pre-Oligocene substratum made of volcano-sedimentary and metamorphic rocks, with Cretaceous to Eocene plutonic intrusions (Dingman and Galli, 1965; Salazar et al., 1998; Blanco et al., 2012a; Scheihing et al., 2017). The other model (Magaritz et al., 1989, 1990; JICA-DGA, 1995) considers a recharge from the Altiplano watersheds (Salar del Huasco) towards Pica and the Central Depression through deep faults and fractures. This hypothesis, often considered “unlikely”, has been refuted in two recent articles (Uribe et al., 2015; Scheihing et al., 2017).

 

Fig. 4. Lithostratigraphic column of the study area (modified after Blanco et al., 2012b).

Scheihing et al. (2017), based on a new analysis of a seismic reflection profile carried out by the National Petroleum Company (ENAP) in 1960, propose that the emergence of Pica thermal springs is induced by plutonic intrusions of Cretaceous to Eocene age that penetrated the Mesozoic basement. These intrusions have, in the long term, destabilized the overlying Oligocene formations (Sagasca Member) and allowed the development of an important system of vertical fractures. The water circulating in the Sagasca Member (OMap 1) uprises to the surface through this system of fractures and feed the thermal springs and the Pica aquifer.

2.2. Methods

The first step of the study consisted in the review of the literature mentioning the socavones of the Pica area, the interview of key informants among the Pica and Matilla inhabitants and the review of Google Earth Satellite images. The key informants interviewed included staff from the Municipality of Pica, the responsible of the Museum of Pica and owners of lands with socavones. The second step was the survey of all the elements belonging to the socavones and visible on the ground surface (entry points, shaft wells, wells, reservoirs, open channels) with an assessment of the access to the underground tunnels. This was followed by the geo-referencing survey of all those elements (third step). The fourth step consisted in the exploration and mapping through a topographical survey of the galleries that were accessible. For this study, tunnels have been accessed from their exit point or from one of the shaft wells when the exit point was blocked. In some cases, it has been necessary to abseil down the shaft wells with ropes and gear. In parallel to the exploration, a geophysical prospection with electric method was carried out (fifth step). Finally, geological and hydrogeological studies of the socavones were conducted (sixth step). Steps one to five were undertaken from November 2014 to January 2015 and the field campaigns of the sixth step were in July 2017 and January 2018.

2.2.1. Gallery mapping

An underground topographical survey of the galleries was done using hand-held instruments. The distance was measured with a Stanley TLM 330 laser distance measurer and the section dimensions (height and width) combining a traditional tape with the laser one. The bearing and slope were measured with a Suunto Tandem compass and clinometer. A total of 3,072 stations were measured for an overall distance of 14,537 m of tunnels. The drawing data was processed with Visual Topo 4.7 software.

2.2.2. Geophysical survey

An underground gallery represents a sub-superficial empty cavity inside a sedimentary formation. The difference between the air (very resistive to insulator environments) and the sediments (relatively conductive environment) produces a measurable resistivity contrast between these two domains. However, the stress field and associated deformation, causing fractures, and in some case collapse of underground cavities, well documented in the mining industry and tunnels buildings (Terzaghi, 1946), may produce a much larger zone of influence of relatively resistive domain above the cavity. This is a highly permeable domain that allows the efficient transport of fluids, as clearly demonstrated by the crystallization in the walls and roof of the socavones (see section 3.3). Therefore, the relatively dry and resistive domain is likely larger than the socavón itself, perhaps 2-5 times. Water percolates gravitationally downward where, if still available, it can show up as a relative conductive body. This conceptual model is expressed in figure 5. Thus, the use of the direct current (DC) or electrical tomography resistivity (ERT) geoelectric method appears to be an appropriate methodology to identify the underground galleries.

 

Fig. 5. Conceptual model of the resistivity response of a socavón: A. Above the socavón, a wide permeable domain, product of the stress concentration by the free surface of the socavón, with a tentative maximum size of 4x5 m; B. Below the socavón, if still present, a water reservoir or a humid zone with a relatively conductive domain.

The method consists of the installation of several electrodes, which are used to inject direct current I  (between two electrodes) and measure the potential difference V in the other 15 pairs of electrodes. This configuration is repeated interchanging the potential-current electrodes, modifying in this way the geometry of the current path and associated iso-potential lines. Using this methodology, we were able to map the resistivity distribution along the profile and at different depths of the substratum. The current-potential observations are represented in terms of the apparent resistivity ρ which is the integration of the in situ resistivity of the substratum. The physics behind this relation is based on the direct current approximation of Maxwell’s equations better known as Ohm’s law (see a thorough description of this derivation in Telford et al., 1990). This physical relation provides a simple mathematical expression to determine the apparent resistivity ρ in terms of the observations (current I and voltage difference ∆V; equation 1).

 (1)

The geometrical factor G depends on the relative location of the current electrodes (r₁, r₂) and the potential difference electrodes (r₃, r₄).

Knowing the apparent resistivity, we can then determine the resistivity of the geological units by 2D modelling. In addition, due to the highly contrasting resistive response of the cavities (very resistive) and the surrounding geology (relative conductor), we can interpret the 2D resistive modelling image in terms of geological units-cavities configuration. Even though this geophysical technique is quite powerful to image the underground geo-electrical distributions, it has some limitations for this application. The most critical problems are: 1. If the cavities are very small (less than 2 m²) or at a depth greater than 30 m, the method is unable to resolve due to the very small associated signals; 2. when the tunnel is full of water, the premise of a contrasting geo-electrical response between the cavity and the surrounding geology is no longer valid, due to the fact that water in this environments is always a conductive media. Using the model described in figure 5, the influence of the socavón should be greater than 2 m², perhaps as large as 10 m². In this case the chances to identify the socavón become higher.

The geo-electrical profiles were conducted perpendicular to the supposed route of the socavón. Between two profiles, a straight line was traced in order to join the two identified cavities or lumbreras. The error on the route is around 10 m on each side of the identified line. Using this methodology, only the main galleries were identified.

The geophysical deployment considers the use of the TIGRE instrument with 32 electrodes separated at a constant distance of 5 m, with a Schlumberger-array geometry. For each pair of current injection and potential measurement, we have made three measurements to analyse the dispersion of the data. We only accept data with less than 10% of variability. In practice, to inverse the data, we use Zondres 2D software (http://zond-geo.com/english/zond-software/ert-and-ves/zondres2d/; last visit 22/07/2020) for resistivity imaging with the Occam algorithm (Constable et al., 1987) to carry out the inversion effort and find the best solution. In total, 41 geo-electrical profiles were made.

2.2.3. Geo-referencing survey

The position (latitude, longitude and height) of the elements of the socavones that were visible on the ground surface (exit points, shaft wells, wells, reservoirs) was georeferenced with centimetre accuracy using a geodesic GPS (Trimble R6 with double frequency). The point used as reference was the geodesic vertex Matilla 2 of the Ministry of Public Properties. In total, 154 elements were georeferenced. Due to accessibility problems, 15% of the elements were georeferenced with a navigator GPS (with meter accuracy).

2.2.4. Geological and hydrogeological study of the socavones

The geology of each socavón has been mapped. All springs have been registered as well as water levels in the galleries along with physicochemical measurements. Chemical analysis of nine springs in the socavones were carried out by the Montpellier HydroSciences laboratory by ion chromatography (anions) and ICP-MS (cations and trace elements). As a result, a piezometric map and hydrogeological profiles have been developed as well as a new hydrogeological conceptual model.

3. Results

In the area of Pica, including Matilla and Puquio Núñez, 34 socavones have been inventoried. Only 20 galleries are accessible or partly accessible so their exploration has been possible along with the realisation of a topographical survey, completed by the geo-electrical prospection of inaccessible sections for five of them. In some socavones, the water built up and fill all or a big part of the tunnel. In those cases, it has not been possible to explore and map the drown sections (San Isidro, El Carmen y Concova). Four socavones are entirely inaccessible but have been identified through a geophysical survey. Ten galleries could not be identified in the field. 85% of the galleries have been identified through exploration and 15% through geophysical survey (Fig. 6).

 

Fig. 6. Map of the identified socavones of the Pica area. Insert A shows Puquio Núñez socavón located 10 km south of Pica. B. Socavones located in Pica and Matilla Oasis. A-A’ and B-B’ cross-sections: Location of the geological and hydrogeological profiles of figure 14. Purple dotted line: Inferred gallery. PNU: Puquio Núñez; LOR: Loreto; CAR: El Carmen; QUI: La Quinta; CON: Concova; SRA: Santa Rosa; SCR: Santa Cruz; SRI: Santa Rosita; ALG: El Algarrobo; COM: Comiña; SE1: Santa Elena I; SE2: Santa Elena II; SIS: San Isidro; SAU: El Sauque; SMA: San Matías; GOL: El Gólgota; CVI: Cementerio Viejo; MOL: Puquio El Molle; BOT: Botijería; BE1: Buena Esperanza I; BE2: Buena Esperanza II; JMA: Jesús María; MIR: Miraflores; CNE: Cementerio Nuevo.

3.1. Identification of inaccessible socavones through geoelectric prospection

In total, 41 geo-electrical profiles were deployed. Poor ground conditions, with contact resistance above 1,000 ohm-m, hamper a good quality results. Nevertheless, we were able to obtain reliable data in some sections, which allow to test the proposed conceptual model (Fig. 5). Figure 7 shows two examples in which the galleries are most likely detected. The observation is represented in the upper panel of figure 7a and b, and the 2D model inversion section is represented in the lower panel, whereas the model response is shown in the middle panel.

 

Fig. 7. A. Santa Elena Socavón. B. La Quinta Socavón. Upper panel: pseudosection of the observations. Middle panel: model response. Lower panel: 2D model inversion section (in red circle, the interpreted socavón in agreement with the conceptual model). The vertical scale in the pseudo sections is apparent depth and the coloured resistivities are apparent resistivities (an integral of the resistivity between the current injection point and the voltage measured point). Observation and model response should match if the model is correct. The inversion section depth is in meter and resistivity corresponds to the resistivity distribution in the space.

Geoelectrical observations are represented as apparent resistivity pseudo-sections. Apparent resistivity implies an integration of the real resistivity in the space, and the pseudo section is an apparent estimate of the real depth. In order to translate these observations into depth-dependent resistivity, we need to apply 2D models that fit the data, formally representing a model inversion (i.e., Parker, 1994). The galleries were detected in almost all the cases and their lengths were estimated. Model response is a test of the goodness of the inversion process and average misfit below 20% is consider a reliable solution in this case, considering the middle to poor quality data available. In the inverted sections of figure 7, we interpret the socavón response as relative resistive domains (200-300 ohm-m), surrounded by a conductive domain one order of magnitude less resistive (30-50 ohm-m). The size of this resistive domain is larger than the expected socavón size, fitting the size and rounded shape of the proposed model (Fig. 5). The model response of Santa Elena socavón (Fig. 7a) indicates a resistive domain of 8-12 m diameter at depths below 10 m, a bit higher than expected by the conceptual model (Fig. 7). However, no clear conductive domain is identified underneath, eventually due to the lack of humidity and/or the loose of resolution at depths greater than 20 m. For the case of La Quinta socavón (Fig. 7b), the same configuration in the inversion model is observed (resistive socavón response (200-300 ohm-m) inside conductive domain (30-40 ohm-m)). The main difference is the size and depth of the interpreted socavón, in this case 4-8 m diameter at depths around 5 m. The size in this case is more in agreement with the conceptual model of figure 5. There upon, it is necessary to point out that shorter wavelengths’ bodies can be identified at shallower depths. Thus, it is expected that smaller features can be correctly detected at these levels. As it is evident in the model results shown in figure 7, the geoelectrical representation of the socavón is not necessarily unique, other anomalous domains are also likely candidates. In the future, other indirect geophysical approaches can complement the geoelectrical technique used here, for instance georadar. Nevertheless, the results are in agreement with the conceptual model (Fig. 5 and section section 2.2.2) and evidence a socavón in the selected examples.

3.2. Characteristics of the socavones at Pica area

The 24 socavones identified sum up a total gallery length of 18.2 km (main tunnel and side branches; Table 1). Taking into account the unidentified galleries, the total network of the socavones is expected to cover a distance of 20 km.

A complete description of the physical feature of the socavones of Pica area is given in Appendix 1. The most original feature of the socavones of Pica area, compared to the filtration galleries in other regions of the world, is the shaft wells. With the exception of the socavón of Loreto, they are not located vertically over the main tunnel but either on the right or on the left side of the galleries, without any apparent logic. As well the socavones do not have “mother wells”, again with the exception of Loreto.

3.3. Geological and hydrogeological study of the socavones

The socavones of Pica area are dug in Pleistocene-Holocene alluvial deposits, which consist of poorly consolidated sands with intercalated layers of clay and silts. This formation underlies the modern and active wind deposits and overlies oligo-miocene alluvial and volcanic formations (Blanco et al., 2012a; Blanco et al., 2012b). Almost all the socavones have a SW-NE orientation, running parallels to the direction of the maximum topographic gradient (Fig. 6).

One of the main findings of the geological study of the socavones is the identification of outcrops of Tambillo ignimbrite (MiiT, in Fig.3) in all the socavones located in Matilla (Fig. 6), over the (inferred) Longacho Flexure, with their exit point located in the escarpment on the western side of the flexure (San Matías, Cementerio Viejo, Puquio El Molle) (Fig. 8). From their exit point, those galleries are dug in unconsolidated sand and, after a few tens of meters, they come across few meters of Ignimbrite. Then, the galleries are dug in layers of clay intercalated with poorly consolidated sand (collection section). In the socavón Puquio El Molle, the contact between the ignimbrite and sand deposits on the eastern side of the ignimbrite outcrop shows a contact angle of 55° (non-erosive contact). In most of those cases, the hardness of the ignimbrite obliged the workers to continue the excavation overriding it, one or two meters higher than the initial level of the main gallery (Fig. 8c and d).

 

Fig. 8. Ignimbrite outcrops in Puquio El Molle (A), Cementerio Viejo (B), San Matías (C) and Loreto (d).

The socavones located at the northern and southern edges of the area (Loreto and Puquio Núñez, LOR and PNU; Fig. 6) show similar geological pattern, although with some differences. Loreto is not located over the Longacho Flexure but two kilometers to the East. The gallery, after layers of clayey sand and intercalated layers of clay, comes across an ignimbrite layer with an important spring (LO05) flowing through a fracture with a N113 direction. To the East, the gallery follows the ignimbrite layer, which obliged the workers to continue digging overriding it, two meters higher than the initial level of the gallery, up to the mother well at the end of the gallery (Fig. 8d). The presence of the ignimbrite two kilometres east of the Longacho Flexure is an evidence of the presence of another similar structure which do not show on the surface. The structure is confirmed by a gravimetry profile realized by the General Water Department (DGA, 2012) where a basement height is identified at less than 50 m below the surface right down the Loreto socavón. In Puquio Núñez, the tunnel did not cross ignimbrite rocks (probably much deeper at the southern edge of the flexure) but important layers of clay intercalated with poorly consolidated sand in the conduction section. The socavones located between Pica and Matilla are dug in homogeneous and poorly consolidated sand layers, evidence of the presence of a deep sedimentary basin, as well confirmed by gravimetric profiles (DGA, 2012; Con Potencial Consultores, 2013).

Another important finding resulting from the exploration of the socavones is the observation of important layers of clay in the socavones, especially in the sections of the galleries located on the eastern side of the ignimbrite outcrops (Fig. 9). This is confirmed by the stratigraphic columns recorded on deep boreholes (about 100 m deep) between Pica and Matilla (Con Potencial Consultores, 2013) and shows the prevalence of layers of clay in Pleistocene-Holocene alluvial deposits.

 

Fig. 9. Layers of clay in the socavones San Matías (a) and El Sauque (b).

Finally, the description of Tambillo ignimbrite outcrops in the Quebrada of Quisma and Matilla (Figs. 3 and 10) shows that the ignimbrite is strongly fractured, owing an important secondary permeability.

Regarding the groundwater, the exploration of the socavones allows to identify two different types of springs in the galleries: i. Emergence by intersection of the piezometric level in the unconsolidated sands of the Pleistocene-Holocene alluvial deposits with the galleries, which drain the aquifer (Fig. 11A); ii. overflow springs through fractures in the Tambillo ignimbrites (socavón Loreto) or sandstones and conglomerates of El Diablo Formation and Imagua Member (thermal springs of Pica, Fig. 11b).

 

Fig. 10. Ignimbrite outcrops in the Quebrada of Quisma (a); Matilla (b).

 

Fig. 11. Springs (a) in the unconsolidated sand deposits in San Matías; (b) in ignimbrite fracture in Loreto.

The physicochemical measurements show that the source of Loreto socavón (LO05; Fig. 6) has the highest temperature of Pica-Matilla oasis (34 °C). The thermal springs of Pica (Resbaladero RE01, Concova CN01; Fig. 6) have a temperature of 32 °C. However, these have a very low salt content for the region (conductivity ~330 μS/cm) while Loreto show a high salt content (conductivity ~2200 μS/cm). The springs in the socavones of Matilla have a salt content between these two extremes (conductivity ~1100 μS/cm) and a temperature of approximately 27 °C (Table 2, Fig. 6).

The analysis of the major elements of nine springs in the socavones of Pica (Fig. 12, Table 2) shows two different groups: 1. sodium bicarbonate to mixed waters in Pica and Puquio Núñez area (Miraflores MI01, Resbaladero RE01, Concova CN01, Puquio Núñez PN03); and 2. sodium sulfate waters in Loreto and Matilla area (San Matías SM06, El Sauque SA02, Loreto LO05).

 

Fig. 12. Piper diagramme of the springs of Pica.

These hydrogeochemical facies have already been described by Grilli et al. (1999). The sodium bicarbonate facies of the thermal springs of Pica is similar to those found in the springs of the northern, western and southern edge of the Salar of Huasco and is typically observed in waters circulating in volcanic  rocks such as ignimbrites (Grilli et al., 1999; Aravena, 1995).

In many galleries, precipitation of calcium carbonate (CaCO₃) covers the walls and floor of the tunnels in different proportion. Some tunnels are totally covered with calcium carbonate, as El Carmen socavón, where CaCO₃ (Fig. 13a and b) precipitates in the form of Aragonite, as it has been observed also in some wells of Pica. Calcium carbonate precipitation is a result of the degasification of excess dissolved carbon dioxide in groundwater when it seeps from the aquifer into the empty gallery (Banks and Jones, 2012). Additionally, in five socavones, a sedimentation of manganese oxide (MnO) has been observed on the walls, floor and sometimes ceiling of the tunnel. When both sedimentation occurred (CaCO₃ and MnO), the tunnel sides are covered first by manganese oxide, itself covered by Calcium Carbonate. The height of sediment on the wall shows the past water seepage and level in the gallery. The fact that some galleries show sedimentation, and others do not, shows different groundwater composition. Indeed, precipitation of CaCO₃ occurs in the galleries were ignimbrite has been found and groundwater circulates through fractures. Some socavones show abundant traces of roots, replaced by iron hydroxide, carbonates or silica (Jesus María, El Sauque and Botijería), related to the paleo-wetland facies of Paleocene-Holocene deposits on the eastern margin of Longacho Flexure (Blanco et al., 2012b). It is also possible to find stalactites (but no stalagmites) as well as small pisolites (pearl caverns) and tiny gours or rimstone dams’ formations on the gallery’s floors. The stalactites are mainly soda straw type with 5-6 mm thick and up to 30 cm long. Other drapery, curtain or bacon rind stalactites, also small size, are visible (Fig. 13c).

 

Fig. 13. a y b. Calcium carbonate covering carved steps and iron ladder in El Carmen socavón. c. Stalactites in El Sauque socavón.

3.4. State of the socavones today

Although only seven socavones, out of 24, still discharge water today (Fig. 6), 17 have groundwater flowing in some sections of the tunnels (70%). Nevertheless, the water level is today much lower than it has been in the past, as evidenced by the marks left by the water on the tunnel sidewalls. Billinghurst (1893) and Bruggën (1918) reported a similar total discharge of the socavones, around 40 l/s. This flow was much lower than the total discharge from the springs of the oasis, reported to be 92 l/s in 1865, 119 l/s in 1918 and later on   53 l/s (Dingman and Galli, 1965; Fritz et al., 1981; Magaritz et al., 1989). The visual estimation of the groundwater flow in the active galleries today gives a total discharge at least 50% lower than in 1918. In three socavones, water fills the whole tunnel section (Carmen, San Isidro, Cementerio Nuevo). This may be due to the blockage of downward tunnels by sediments so the groundwater builds up to the water table level.

Although the agriculture in the oasis of Pica has expanded in the last decade, most of the socavones are today abandoned. Due to the growth of both Pica and Matilla towns, and the absence of knowledge about the localisation of the socavones, several infrastructures have been constructed over them. In particular, the center of Pica has developed over the gallery El Carmen leading to the subsidence of the ground and formation of sinkholes. 

In some galleries, part of the tunnel has collapsed. Although earthquakes with magnitude over 7 Mw have occurred in the region in the last decades (1976, 2005, 2014), they did not cause a major destruction of the socavones of Pica area. Nevertheless, the impact of recent earthquakes is visible in some galleries, in part because they are not anymore maintained. In general, main galleries are still in excellent conditions although exit points and/or shaft wells may be deteriorated, collapsed, or covered up by sand or garbage.

Only seven socavones are still in use (Miraflores, Concova, Loreto, Santa Rosita, San Matías, El Sauque and Botijería), mostly for irrigation purposes, with the exception of Santa Rosita used by the regional water supply company. Miraflores, Concova, along with the thermal spring of Resbaladero are still managed collectively through farmers associations, as it was traditionally. The water is distributed among the farmers through a canal network and strict timing.

Nevertheless, today in the oasis, crops are mainly irrigated through shallow wells (around 30 m deep) or borehole (over 100 m).

4. Discussion

The filtration galleries of Pica area share many common features with the ones described in other parts of the world. However, they also have distinctive features that make them unique in their kind. As asserted by Villalobos (1979), Chilean filtration galleries represent a local development of the ones found in Spain and North Africa. One of the main differences is the shaft wells structure (with the exception of Loreto). A hypothesis for this type of shaft well construction locally called lumbreras is that the area is a windy and sandy desert. If the well is dug vertically over the main tunnel, the sand may accumulate directly in it, obstructing the water flow. If the well is replaced by a diagonal tunnel, the sand accumulates in the branch gallery before reaching the main tunnel. The accumulation of sediments in the main tunnel reduces the water flow and increases the need of maintenance. Today, the main tunnels are not blocked with sediments from the surface although they are abandoned since years. In a few cases, it has been necessary to clear out the tunnels and remove the sand in order to continue the exploration, but in general, the sediments have accumulated in the lumbrera. Another hypothesis is that it is more difficult to dig a well vertically over an underground tunnel as it entails levelling expertise.

Another characteristic, which distinguishes the socavones of Pica is the absence of mother wells (except Loreto). It may be the reason why the main galleries are not straights lines between the exit point and the end (where the mother well is supposed to be located and dug first). The only exception is again Loreto, which seems to have been built in the rule of the art of filtration galleriesconstruction. This could be an evidence that Loreto was the first socavón built in the area.

Those differences observed in Pica may be, on one hand, an adaptation to the climatic context and local geology (important accumulation of sand transported by the wind, presence of a hard ignimbrite layer and earthquakes). On the other hand, it may be due to a lack of expertise of the workers who built the socavones compared to the filtration galleriesMasters in Iran, China or other places, where hundreds of filtration galleries were built, some with tens of kilometres long. This hypothesis supports Bruggën (1918) observations of several galleries with water built up because of uneven tunnel slope, or galleries in bad state (collapsed) affecting the discharge flow of the galleries. The short distance between galleries, probably affecting the discharge flow, may be another evidence of the lack of expertise in the socavones construction.

The alluvial fans of the Central depression are an ideal setting for the development of socavones of longer distance. However, this technique has not been developed outside of the Pica area although there has always been irrigated agriculture in the Pampa del Tamarugal. Different hypothesis can be advanced and discussed: the surface water flow, although low, was always sufficient for covering the needs of the local inhabitants or expert knowledge lacked for the construction of longer and deeper galleries.

The geological and hydrogeological information generated through the exploration of the socavones, completed by stratigraphic information of deep boreholes and gravimetry profiles (DGA, 2012; Con Potencial Consultores, 2013) allowed for the elaboration of two W-E geological and hydrogeological profiles (Figs. 6 and 14). The presence of the Tambillo ignimbrite on the western edge of the Longacho Flexure, in the galleries located over it and its absence on the eastern side, is an evidence of the presence of the flexure. The ignimbrite outcrops highlight the top of the anticlinal, which is induced by a reverse fault with a western dip. It confirms the proposition of Labbé et al. (2015) and refutes the interpretation as a normal fault of Dingman and Galli (1965) and Scheihing et al. (2017). Victor et al. (2004) interpret the structure as a reverse fault but with an eastern dip. The fault affects only the Mesozoic (Jurassic) bedrock and folds the Sagasca Member (OMap 1) and Tambillo ignimbrite (MiiT). The Imagua Member (OMap 2) and El Diablo (Mmd) Formation are not present on the top of the anticlinal as they end in bevel on the eastern side of the flexure zone (Victor et al., 2004; Labbé et al., 2015).

 

Fig. 14. Geological and hydrogeological W-E profiles of the Pica aquifer. The location of the profiles is given in figure 6.

The fracturation of the Tambillo Ignimbrite and the continuous groundwater flow over the Longacho Flexure (observed in the socavones of Matilla and confirmed by the piezometric map, figure 6 show that the Tambillo ignimbrite is not the formation that limits at its base the alluvial aquifer of Pica, but the layers of clay of the Pleistocene-Holocene alluvial deposits.

A similar structure (anticlinal), located East of the Longacho Flexure and parallel to it (N-S direction) induced the outcrop of the Tambillo Ignimbrite in the socavón of Loreto and the presence at shallow depth (~50 m) of the pre-Oligocene basement. We interpret this structure as the extension, to the north, of the anticlinal and reverse fault, with an eastern dip, inducing the emergence of the Pica thermal springs in the conglomerates of El Diablo Formation (Fig. 14; Victor et al., 2004; Blanco et al., 2012a; Blanco et al., 2012b; Blanco and Tomlinson, 2013).

The physicochemical analysis of the springs in the socavones allow us to identify two groundwater poles: i. Groundwater with low salt content (conductivity ~320 μS/cm) and thermal (~32 °C) in Pica (located on the eastern border of the aquifer); and ii. Groundwater with higher salt content (conductivity ~2,000 μS/cm) and thermal (34 °C) in the northern zone of the aquifer (Loreto; Fig. 13). Between the two poles (central and western zone), the groundwater ha a salt content that can be interpreted as a mixing between these two poles (conductivity ~1,100 μS/cm). The lower temperature of the latter (~27 °C) is probably due to the cooling of groundwater from the two poles in the shallow aquifer of Pica which may, additionally, receives water from infiltration of irrigation waters.

These results allow to review and complete the existing conceptual model of the Pica aquifer, particularly the origin of flows recharging the aquifer. This work confirms the first recharge model (Dingman and Galli, 1965; Fritz et al., 1981; Suzuki and Aravena, 1985; Salazar et al., 1998; Grilli et al., 1999; Rojas et al., 2010; Jayne et al., 2016; Scheihing et al., 2017) but proposes an additional recharge mechanism. Findings show that two processes control the recharge of the Pica aquifer:

1. On one hand, as proposed in previous studies, a recharge from precipitation in the Altos de Pica area, circulating through the Cenozoic cover (Sagasca Member, OMap1) and emerging at Pica (thermal springs) through the fractures affecting the Cenozoic cover. Those fracture may be generated by the fault of Chintaguay that affects the pre-Oligocene basement and strongly folds the Cenozoic cover and the plutonic intrusions of Cretaceous to Eocene ages. This groundwater has a very low salinity and a thermal footprint that corresponds to its depth of circulation (Scheihing et al., 2017). Groundwater flow has a general E-W direction.
2. On the other hand, a recharge from the pre-Oligocene basement, of groundwater inflow with a high salt content (conductivity ~2,000 μS/cm) and high temperature (34 °C). Water emerges through fractures without displacement affecting the horizon of ignimbrite overlying the pre-Oligocene basement (the OMap 1 and 2 members of the Cenozoic cover are probably absent due to the basement height). Similar structures can be observed in the Quebrada de Tarapacá (Viguier, 2016). The main groundwater flows have a rough N-S direction.

A third group is represented by the groundwater of Matilla, which seems to be a mixing between the two types of groundwater described above because located at the convergence flows from the north (Loreto) and from the east (Pica). Based on those findings, a new conceptual model has been elaborated (Fig. 15).

 

Fig. 15. Hydrogeological conceptual model of the Pica aquifer.

Today the galleries are abandoned and at risk to disappear both physically and from the local population memory, once all exit points and shaft wells will be buried or have collapsed. A lack of maintenance may have led to a reduction of the discharge flow (sedimentation on the tunnel ground, mineral deposits on the tunnel sides reducing seepage, fear of earthquakes and tunnels conditions), or too much and too close galleries affected the flow. Some may have been seriously damaged by earthquakes or a major portion of the tunnel may have collapsed, again reducing the discharge of the gallery. Eventually, the socavones may have been abandoned because the water table of the aquifer fell down, reducing the discharge of the galleries. The rise of the number of wells and borehole in a relatively small area (the oasis) may have led to the rapid drawdown of the aquifer and the drying up of the filtration galleries. 

We believe that the socavones of the Pica area have still a role to play in the modern world. They first deserve to be preserved because they represent a water and geoheritage of one of the driest places on Earth, as well as for their unique characteristics and the human effort engaged in their construction. Some of them could be habilitated so they could be visited for cultural, educational and scientific purposes. In addition, they can still play a role in groundwater management of the Oasis of Pica. The evolution of the groundwater level in the galleries can be used as an indicator for aquifer management. As most of the wells are private and in use, they cannot be used for the monitoring of the water table. Eventually, the abandoned shaft wells and tunnels could be used for managed aquifer recharge. Either surface runoff or reused water could be injected into the shaft wells, so empty tunnels of abandoned socavones will be filled with water, which will in turn slowly infiltrate into the aquifer.

5. Conclusions

The underground exploration, topographical survey and geo-electrical prospection of the socavones of Pica area have allowed identifying and describing 24 socavones with 18.2 km of galleries, that is 70% of them. We expect the other 30% to be completely buried. Even though, it deserves further research.

Our study came across various limitations. During the exploration, some galleries were not explored because of high risk of collapse. Additionally, some supposed galleries (informed by local population) investigated with geo-electrical survey were not found. Although it is possible that the galleries are totally buried, it is also conceivable that gallery is too small or too deep to be detected by the geo-electrical method. Our first attempt to indirectly characterize socavones by geo-electrical geophysical techniques delivered promising results, showing a pattern of resistive domains (200-300 ohm-m) inside a more conductive area (one order of magnitude less). But it is still necessary to improve the application of the technique in order to obtain more reliable results. Future challenges are related to an efficient methodology to improve the electrode contact resistance, and the capacity to detect small objects (2-5 m) at depth larger than 10 m. On the other hand, the use of complementary techniques, like Georadar, can also improve the capabilities of indirect tools to detect cavities.

The study of the socavones of Pica-Matilla provided a unique insight and new data that contribute to the understanding of the Pica aquifer and hydrogeological processes in the Piedmont area and Central Depression. It leads to the proposition of a new conceptual model. The base of the aquifer of Pica corresponds to the clays of the Pleistocene-Holocene alluvial deposits. It is recharged, on one hand, through fractures and groundwater flows within the Altos de Pica Formation (Sagasca Member) from the Altos de Pica area (E-W flow). On the other hand, this work identified another recharge mechanism from the the pre-Oligocene substratum (N-S flow) through fractures within the Tambillo ignimbrite in the northern part of the aquifer.

The information provided by this research will allow authorities to take appropriate measures for protecting existing infrastructures from sinkhole as well as for land-use planning of the future oasis development. But, above all, it seeks to encourage the preservation of the socavones -an ancient water supply system of arid and water-stressed areas- as water and geoheritage; as well as their reuse for cultural, scientific and water management purposes. Beside the abandonment of most of the socavones today, we believe that they could still have a role to play in the groundwater management of the oasis for groundwater monitoring and managed aquifer recharge.

Acknowledgments
The exploration, mapping and geophysical survey were carried out thanks to a project implemented by the Water Resources Research and Development Centre (CIDERH) and Diedro and funded by the Municipality of Pica, co-funded by CONICYT project R09I100 and the Regional Government of the Tarapacá region (Chile). The geological and hydrogeological studies were funded by Carpe Science, the ECOS-CONICYT project C14U013 and the University of Montpellier (Hydroscience laboratory). We would like to address special thanks to E. O’Ryan from Museum of Pica and to the inhabitants of Pica and Matilla.

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Appendix

Description of physical characteristics of the filtration galleries socavones of the Pica area

The filtration galleries of Pica, known as socavones, are thought to have been built in the late sixteenth century by miners, although not definite evidence has been produced and the earliest mention dates back to 1718 (Barnes and Fleming, 1991)

1. Physical features of the socavones

Almost all the socavones have a SW-NE orientation, running parallels to the direction of the maximum topographic gradient. The only exceptions are Botijería (near NNE-SSW direction) and La Quinta (which turns with a right angle from its initial E-W direction). Beside the general SW-NE direction, the socavones are not straight lines between the exit points and the end of the main gallery but rather a curvy path.

The longest socavon (main tunnel) in the Pica area is Comiña with 2,435 m (Table 1). The shortest is El Algarrobo with 27 m. Six socavones have an extension over 1,000 m (Comiña, El Carmen, Buena Esperanza II, El Sauque and San Isidro). For both Comiña and El Carmen, a section in the middle part of the galleries could not be neither accessed nor identified through geophysical survey so the length was estimated approximately.

The topographical survey identified 227 side branches in the 24 socavones (Table 1), with a total lenght of 2,480 m. For the ones explored through geo-electrical survey, only the main tunnel was identified. So, 12 galleries (Miraflores, El Carmen, Jesús María, La Quinta, Concova, San Isidro, Santa Elena I, Santa Elena II, Comiña, Santa Cruz, El Gólgota y Buena Esperanza I) probably have a total gallery length higher than specified in table 1.

Besides the underground tunnels, the socavones have also a number of elements that are visible on the ground surface. In the Pica area, 154 points related with the socavones were identified in the field and georeferenced. Those points are either shaft wells (called lumbreras, which literally means luminary), exit points, wells or reservoirs (Fig. 1A).

 

Fig. 1A. Map of the identified socavones and elements of the socavones visible on the ground surface of the Pica area. The area of Puquio Núñez is not represented on the map. A. Zoom of Comiña socavón. Blue line: socavón identified through direct exploration. Green line: socavon identified through geophysical survey. B. Socavones located in Pica and Matilla Oasis. Dotted line: inferred gallery. Red dot: Lumbrera. PNU: Puquio Núñez; LOR: Loreto; CAR: El Carmen; QUI: La Quinta; CON: Concova; SRA: Santa Rosa; SCR: Santa Cruz; SRI: Santa Rosita; ALG: El Algarrobo; COM: Comiña; SE1: Santa Elena I; SE2: Santa Elena II; SIS: San Isidro; SAU: El Sauque; SMA: San Matías; GOL: El Gólgota; CVI: Cementerio Viejo; MOL: Puquio El Molle; BOT: Botijería; BE1: Buena Esperanza I; BE2: Buena Esperanza II; JMA: Jesús María; MIR: Miraflores; CNE: Cementerio Nuevo.

The identification of the main tunnel where there are many side branches was sometimes complex. In some cases, the main gallery was identified because an iron sign with the mention matriz (that can be translated as principal from informal Spanish) was found. Probably the iron-sign helped the orientation of new workers or in case of emergency purposes. In other cases, the main gallery was defined based on its aspect of spine, or because it is the longest or the gallery with the last shaft well.

Many socavones have side branches in the water production section, especially at the end of the main gallery (Fig. 1A). The discharge flow of the socavon can be increased by digging side branches that feed into the main tunnel.

The tunnels are generally narrow and tall with a regular and average width of 0.8 m. This is slightly wider than the shoulders’ width of an adult, which is not too narrow for the gallery to be access comfortably and not too wide, which would mean unnecessary digging and longer construction time and cost. The height of the tunnels is more variable, 1.8 m on average. Some galleries (or sections) are only 0.5 m high (sections of El Sauque, end of San Matías, one gallery of Jesús María). The maximum gallery height is 7 m in Loreto, Puquio el Núñez and Buena Esperanza II. In those cases, it is likely that the initial tunnel’s ground was dug deeper to increase the gallery’s flow as shown by the niches done in the walls for the lamps, which are now out of reach.

The slopes of the tunnels vary according to the socavones. Most of them have an optimal gradient according to Semsar Yazdi and Labbaf Khaneiki (2017), i.e., between 0.2% and 0.5% (Comiña, El Carmen, Buena Esperanza II). But some galleries have a higher than normal gradient, above 0.5% (El Sauque and Puquio Núñez with 0.9%), even above 1% (Loreto with 1.35% and San Matías, with 2.6%). A higher gradient may cause the erosion of the tunnel ground. In all the galleries with a higher slope, a hard-rocky layer of ignimbrite (volcanic rock originated by pyroclastic flows) is present, except in Puquio Núñez. This is due to the fact that, when the workers came across a layer of ignimbrite, it was probably impossible to continue digging the tunnel. To avoid abandoning the gallery, the only option was to bypass the obstacle. In those cases, workers dug upward at a right angle and then get horizontal again and dug forward so the tunnel carries on over the rocky layer (Fig. 2A).

Fig. 2A. Steps in the main galleries. Left: socavón  San Matías. Right: socavón Loreto.

The main tunnel and side branches end abruptly in general, with two or three horizontal holes which purpose was to increase the draining area and the water flow. The directions and lengths of the side branches are very variable. Many of these galleries were intentionally covered, semi-buried or permanently sealed with stones and few with cement. The reason behind is probably that they were or became dry and were used for the evacuation of sediments (thus avoiding the need to carry back soil extracted up to the surface).

Sometimes the tunnel ground is covered with a channel made of baked clay tiles in the water transport section (Santa Elena II, Comiña; Fig. 3A). This technique was used to facilitate the groundwater flow and prevent filtrations in the water transport section (through the permeable material in which was dug the gallery or through fractures in the hard layers). In recent years, some tunnel grounds have been covered with plastic sheeting or water is conveyed through PVC or cement pipes in order to prevent a loss of flow through filtration (Loreto, San Isidro, Puquio El Molle).

Fig. 3A. Baked clay tiles channel in Comiña socavón.

1.1. Ground surface elements of the socavones

In most cases, downward the tunnel exit point, there is an open channel connecting the tunnel with a reservoir and then with the cultivated land (chacras). Although most of the socavones do not discharge anymore water and the infrastructure and the chacras are abandoned, their remnants are often still visible through Satellite images (Fig. 4A).

Fig. 4A. Satellite view of the ground surface elements of the socavones

Near Matilla, the exit point of the socavones is often located on an escarpment (steeper ground gradient). The workers probably took advantage of those escarpments, which allowed them to dig shorter tunnels to tap the aquifer. If the ground has a steep slope, the tunnel and ground surface intersect sooner (higher difference between the ground gradient and the tunnel gradient), in contrast to a land with a gentle slope, where the gallery has to travel a longer distance to meet the surface (Semsar Yazdi and Labbaf Khaneiki, 2017). Indeed, the socavones which exit point is in the escarpment of Matilla, on the south-western edge of the area, have the shortest galleries, but El Sauque. On the contrary, the socavones located in the middle of the basin (flatter area) have the longest galleries. On the north-eastern edge, the ground slope starts to increase, and again the galleries’ length is shorter (Fig. 2A).

In the area of Pica, parallelepiped blocks of baked clay and cement around half meter high were located on the ground at a distance of 200 m on each side of the tunnel, defining a buffer zone where no activities harmful for the gallery structure and its discharge flow could be carried out. This rule is however disregarded today.

The socavones located in the oasis of Pica are very close to each other. In most cases, they are separated from each other by less than 500 m, and in some cases less than 200 m. As reported by Semsar Yazdi and Labbaf Khaneiki (2017), in Iran, a filtration gallery built in a soft soil should lie at least 1,500 m away from the nearby gallery -and 1,000 m in a hard soil- so they do not affect each other discharge flow.

1.2. The shaft wells

In the 24 socavones, 116 shaft wells were identified (Fig. 1A). Many shaft wells are today in a poor state, collapsed or blocked by sand and/or garbage. In some cases, they have been totally destroyed by the land owners. Therefore, only some of them are accessible. The gallery with the higher number of shaft wells is Comiña (17) as it has the longest main gallery. Then Santa Cruz has 12 shaft wells, followed by Loreto and San Isidro with 10 shaft wells. The shortest socavones have either one or no shaft wells (Cementerio Viejo, Puquio El Molle, Concova, Botijería, Santa Rosita, El Algarrobo). The average distance between shaft wells is 150 m. According to (Semsar Yazdi and Labbaf Khaneiki, 2017), the distance between shaft wells is usually twice the depth of the wells but this rule was not applied in the Pica area.

In Pica, the shaft wells are not located vertically over the main tunnel but either on the right or on the left side of the galleries, without any apparent logic. Actually, in the socavones, the shaft wells or lumbreras are branch galleries connecting the main tunnel to the ground surface (Fig. 5A). They are perpendicular to the main tunnel with a steep gradient and end with a well connecting the gallery to the surface. In order to facilitate the access through the steep slope, steps were carved on the ground. The well is, in general, a few meters deep and with a square shape. It can be up to 9 m deep and exceptionally 20 m deep (El Carmen, which is the deepest socavón). The only exception is Loreto where the lumbreras are vertical wells located right over the main tunnel. As well, exceptionally, some lumbreras are spiral staircases (Santa Cruz or   El Sauque) or a succession of short sections of gallery with turns of 90 degrees. Given that the wells were carved in a very soft material (unconsolidated sand), their walls were consolidated with clay bricks (adobe), or more recently with concrete. Although today many shaft wells are totally covered by sand, fortunately the sediments do not reach and block the main tunnel so far.

Fig. 5A. Typical shaft well (lumbrera) in the Pica area.