Hydro-Stratigraphic Conditions and Human Activity Leading to Development of a Sinkhole Cluster in a Mediterranean Water Ecosystem

Salento Peninsula (Apulia, southern Italy) is characterised by many active sinkholes, which represent the main geological hazard. The stretch of coastline between the village of Casalabate and Le Cesine wildlife reserve is highly affected, with a system of dunes separating the low beach from extensive wetlands, which were subject to uncontrolled urban development after reclamation. The overall morphology is characterized by flat topography, whilst from a hydrogeological standpoint, the mixing of inland freshwater with advancing brackish water favours the higher aggressivity with respect to soluble rocks, and the development of enhanced dissolution (hyperkarst). The relict landscapes within the protected areas still allow for the recognition of actively occurring sinkholes, which cause damage to houses, the road network and infrastructures. In this article the case of Aquatina di Frigole is described, where in the last 15 years numerous sinkholes have formed, with the processes still in rapid evolution. Detailed surveys allow for to identification of the mechanisms of sinkhole formation (suffusion sinkholes), the deriving cluster, and the main hydrogeological links among the different water bodies in the area. Acquatina di Frigole provides an excellent natural laboratory to observe development and evolution of sinkholes, and their relationships with the stratigraphic and hydrogeological elements.


Introduction
Sinkholes [1][2][3] are often at the origin of damage and problems to public safety in karst environments [4][5][6][7][8]. They are among the most frequent geological hazards in karst terrains worldwide [9][10][11][12] and are typically produced at the surface circular to elliptical landforms, characterized by sub-vertical to vertical walls and depths ranging from some cm to tens of meters. The solubility of carbonate and evaporite rocks with the development of karst processes is at the origin of sinkhole formation [2,3], whose mechanisms may develop in different ways according to the local stratigraphy and permeability, the groundwater flow and in fucntion of the modality of outcrops of soluble rocks (directly at the surface, or covered by other, soluble or insoluble, materials). With a variety of mechanisms of a documentation is an essential element in the assessment process of sinkhole susceptibility and hazard, and in the definition of actions for mitigating the related risks. At this aim, we illustrate the case of Acquatina di Frigole, a protected area including a remarkable swamp where a number of sinkholes is presently evolving. To assess the potential danger from coastal sinkholes, to better comprehend the evolution of the process and to verify the likely effects on the environment, the main predisposing factors must be recognized and monitored. In this article, we present an integrated methodology, which is a combination of detailed stratigraphic and geological data with the available hydrogeological information, and the ecology contribution. All of this is integrated by a long archival research that made it possible to find historical maps and to document the man-made works done in the past. This is a remarkable aspect, since in many cases the loss of memory of how man has changed the natural landscape results in incorrect interpretations of the procesess nowadays at work. Based upon such an approach, the main goals of this contribution are addressed toward the above points, and particularly to document the recent evolution (last 15 years) of sinkholes along a stretch of the Adriatic coast, which is quite important for the touristic development of the area. Such a documentation is an essential element in the assessment process of sinkhole susceptibility and hazard, and in the definition of actions for mitigating the related risks. At this aim, we illustrate the case of Acquatina di Frigole, a protected area including a remarkable swamp where a number of sinkholes is presently evolving.

Materials and Methods
Activities carried out in the present article covered a wide range of actions, starting from historical research in local archives, aimed at finding documents and maps to testify the different steps in the process of land reclamation along the Adriatic Apulia. Even though the issue is of interest for both the local cultural heritage and the health problems in the area as well, many documents had to be scrutinized with detail to reconstruct the history. This was done at the Archive in Lecce, but also through the detailed analysis of old topographic maps by the Italian Geographical Army Institute (IGM). This is a very important part of the study, since the present evolution of the landscape is definitely occurring because of the past human works; as for many other types of geological hazards [71,72], keeping memory of the past events, especially in relation to human activities, is

Materials and Methods
Activities carried out in the present article covered a wide range of actions, starting from historical research in local archives, aimed at finding documents and maps to testify the different steps in the process of land reclamation along the Adriatic Apulia. Even though the issue is of interest for both the local cultural heritage and the health problems in the area as well, many documents had to be scrutinized with detail to reconstruct the history. This was done at the Archive in Lecce, but also through the detailed analysis of old topographic maps by the Italian Geographical Army Institute (IGM). This is a very important part of the study, since the present evolution of the landscape is definitely occurring because of the past human works; as for many other types of geological hazards [71,72], keeping memory of the past events, especially in relation to human activities, is fundamental for a proper understanding of the processes working at present.
At the Acquatina di Frigole lagoon, the ecological part of the study was carried out through a number of surveys and observations, aimed at defining the vegetal species therein present and their main characters in the function of the development of the observed karst processes. Geology and hydrogeology were explored through a wider scale survey, in order to gain the best possible comprehension of the geological-structural setting. For this goal, outcomes from the field surveys were integrated by analysis of the available boreholes in the area to define to the best of our knowledge the real stratigraphic and hydrogeological setting in the area.
A multi-temporal analysis was performed on the orthophotos of the Acquatina di Frigole lagoon, from the years from 2006 up to 2019, when extensive work in the field was carried out to check the stages of development of the sinkholes. The orthophoto collection was also used to measure the main features of sinkhole morphometry in the plan (diameter, area, perimeter) and to assess their rate of widening and/or of coalescence. In the field, it was also possible to measure the depth of a selection of the sinkholes.
In February 2019, an unmanned aerial vehicle (UAV; DJI Phantom 4 pro) was used to fly over the area, at a height of 60 m, producing a further orthomosaic with a resolution of 1.57/pix. In July 2019 a R.O.V. (Remotely Operated Vehicle; BLUROV model by Blu-Robotics) was used to investigate the Acquatina di Frigole lagoon. The vehicle was equipped with a full HD underwater camera, termometer, singlebeam echo sounder, and GPS (GARMIN ECHO MAP 72sv). This instrumentation was used to follow in the Acquatina di Frigole lagoon no. 5 continuous survey lines (labeled as tr01, tr02, tr03, tr04 and tr05) parallel to the coast, whilst additional no. 5 survey lines (tr06, tr07, tr08, tr09 and tr10) were carried out in the direction perpendicular to the coastline. Overall, about 1 km was surveyed in this way. The ROV was also equipped for video registration, but this was only locally possible, due to the high turbidity of the water, deriving from the movement of the operator guiding the ROV, which resulted in very poor visibility.
During the survey, along 4 surveyed stretches (respectively with length of 97 m, 274 m, 310 m and 304 m), the depth, water temperature and georeferenced location were recorded. The collected data indicated a maximum depth of 1,2 m in the basin, while the minimum depth is only 0.3 m. The water temperature is in average 29.7 • C (minimum value 29.4 • C, maximum 30.2 • C) at the deepest sites, and slightly higher (average 30.6 • C) in the less deep areas.
The hydrogeological characteristics of the Salento Mesozoic carbonate aquifer allow the marine waters to penetrate the subsoil of the entire territory; these invading marine waters connect the Ionian with the Adriatic Sea, forming a single underground water body, which is at the origin of the severe problems of marine intrusion [85][86][87][88][89].
Meteoric waters infiltrate the subsoil in concentrated form through sinkholes and/or fractures and/or in a diffuse manner when encountering the more porous geological formations. At the base level of freshwater (the sea), outflow occurs along the coast, both in diffuse and concentrated form (springs) [90]. Among the springs, the most important are Chidro [91] and Tara [92] on the Ionian side and Idume and Giammatteo on the Adriatic coast [93], together with the sulphurous springs at Santa Cesarea further south [94][95][96].
The hydraulic behaviour of this part of Salento, characterised by high heterogeneity due to fractured and karstified linestones and the widespread presence of sinkholes, results in channelized flow regimes and fast groundwater flow and transport. The coastal and karst nature further exacerbates the evidence of serious implications on groundwater quantity and salinization, due to climate change and human-related pressures, as a consequence of the overexploitation of the resources for agricultural and domestic activities [81][82][83][97][98][99][100][101][102][103][104][105][106][107].
The shallow aquifers, represented by Oligo-Mio-Plio-Pleistocene sedimentary deposits, are of difficult geometric definition, with sediments characterized by extremely variable types and degrees of permeability: generally permeable by porosity and secondarily by fractures, they can also be partly affected by karst caves or networks, due to the carbonate nature of the clasts. The degree of porosity is conditioned by frequent and sudden changes in the respective percentages of the grain size components, which is why the aquifers overlap aquicludes or pass both laterally and vertically to aquitards.
Geomorphologically, the Salento peninsula is a low-elevated landscape composed of Pleistocene terraces, bounded by NW-SE and NNW-SSE scarps extending from the sea level to altitude of 160 m a.s.l. The marine terraces were produced, since the Middle Pleistocene, by the combined effects of regional uplift and glacio-eustatic sea level changes [54][55][56][57][58] and are overlain by thin calcareous sandstones, locally associated with dunes.
Long stretches of both the Ionian and Adriatic shorelines are dominated by sandy beaches and dunes, alternated to small calcarenite promontories. The latter are covered inland by recent swamp deposits (clays and silts) and by karst residual materials. The main landforms (shorelines, scarps, divides) appear to be strongly controlled in their development by the tectonic lineaments [45,46,63]. At a smaller scale, even minor karst coastal landforms are influenced in their spatial distribution by the main discontinuity systems within the rock masses [108]. The Holocene sea-level rise worked in originating many marshes and lagoons along the Salento coastlines [25,37,[109][110][111][112].
Eastern Salento is characterized for over 35 km by short sandy beaches, bounded by small rock promontories and inland by dunes, progressively disrupted by anthropogenic actions. The dune system separates the beach from the extensive wetlands occupying morphological depressions produced by slight undulations of the bedrock (nucleus of syncline in the Miocene sediments) [29,90,113,114].
The Holocene deposits cover the Miocene-Pleistocene carbonate bedrock [111,114,115]. Freshwater availability favoured the colonization of this area, as documented by recognition, within the Holocene aeolian deposits, of three units: mid-Holocene, Greek-Roman and Medieval age [116]. In the different epochs, alternating stages of mild climate (Bronze Age) and of declining vegetation cover [117], brought also to intense phases of alluviation, and to later renewal of the natural vegetation, probably to be linked to abandonment of rural areas due to the unhealthy environment [117]. In the post-Roman period, the Saracen incursions and the Norman occupation resulted in depopulation of the area [118]. During the Middle Ages, a renewal of agriculture is testified by the sharp decline of shrubland and the high presence of cultivated plants [117]. Later on, between the 15th and 18th centuries, the settlements were scattered because of the Turkish and Saracen incursions, with fortified farmsteads and coastal towers. The population lived upon sheep breeding, cereals and olive cultivation [119], but the economic development was limited by the unhealthy swamps along the coast and the spreading of malaria. Wide abandoned areas, with marshes of limited size that dried up during the dry season, were reported by several authors at the beginning of the Italian Kingdom [120,121]. Libertini [122] identified many coastal marshlands along the Adriatic coast and pushed toward their transformation into agricultural fields through reclamation works. During the first decades of 20th century, wide sectors of the Salento coastlines were actually reclaimed [123,124]. Since the beginning of the 1970s, many coastal marshlands became to be occupied with vacation houses, leading to an uncontrolled urbanization, and, at the same time, originating a highly fragmented landscape, with swamp relicts in the protected areas (Le Cesine, Acquatina di Frigole, Regional Park "Bosco e Paludi di Rauccio") and intervening large sectors occupied by houses, where the original morphological elements of the karst landscape had been cancelled.

The Acquatina di Frigole Site: History
Geographically, the Acquatina di Frigole lagoon is located northeast from the city of Lecce, just north of the Marina of Frigole. Its present configuration ( Figure 2) is the result of the superimposition on the natural elements of significant reclamation works that essentially had a two-fold purpose: hygienic, for the eradication of malaria, and economic, for the exploitation of land to be used for agriculture and fishing.

The Acquatina di Frigole Site: History
Geographically, the Acquatina di Frigole lagoon is located northeast from the city of Lecce, just north of the Marina of Frigole. Its present configuration ( Figure 2) is the result of the superimposition on the natural elements of significant reclamation works that essentially had a two-fold purpose: hygienic, for the eradication of malaria, and economic, for the exploitation of land to be used for agriculture and fishing. The first attempts to reclaim the land started in 1870 by Federico Libertini, who owned most of the land between Torre Veneri and Torre Chianca. Libertini's works consisted of the construction of a network of canals leading into the sea and of the Acquatina di Frigole lagoon itself, an overall system which was intended to drain the waters from the wide marshlands. However, soon, the reclamation works turned out to be too demanding for Libertini, and he had to abandon such challenge, and turned down to die in poverty. Reclamation of the marshlands became again a priority of the government in 1900 when Luigi Libertini, head of the provincial technical office, planned the drainage of wide sectors, including Acquatina. The water was conveyed directly to the sea through canals when the bottom of the marshland was above the sea level. If, on the other hand, it was below sea level, as at Acquatina, the canals conveyed the waters into two tanks, one of arrival and the other of discharge from which, through a pumping machine, the same waters were poured into the sea [122] ( Figure 3). The first attempts to reclaim the land started in 1870 by Federico Libertini, who owned most of the land between Torre Veneri and Torre Chianca. Libertini's works consisted of the construction of a network of canals leading into the sea and of the Acquatina di Frigole lagoon itself, an overall system which was intended to drain the waters from the wide marshlands. However, soon, the reclamation works turned out to be too demanding for Libertini, and he had to abandon such challenge, and turned down to die in poverty. Reclamation of the marshlands became again a priority of the government in 1900 when Luigi Libertini, head of the provincial technical office, planned the drainage of wide sectors, including Acquatina. The water was conveyed directly to the sea through canals when the bottom of the marshland was above the sea level. If, on the other hand, it was below sea level, as at Acquatina, the canals conveyed the waters into two tanks, one of arrival and the other of discharge from which, through a pumping machine, the same waters were poured into the sea [122] ( Figure 3).
Tree species in the surrounding areas were selected based upon their capacity to absorb the remaining water and facilitate soil cultivation. This reclamation system actually turned out to be ineffective because the channels intersected the surficial aquifer, so that, when the dewatering machines stopped working, the water table returned quickly to the initial level. In the early 1920s, therefore, the landscape was still characterized by extensive marshlands, and malaria was fairly widespread [125,126]; even the attempt to eradicate the disease by sending into the Acquatina water thousands of Gambusia affinis (Baird & Girard (1853)), an exotic species from America that had the characteristic of feeding on mosquito larvae, failed [124]. In 1921, the Opera Nazionale Combattenti (ONC) undertook the management of coastal areas (Acquatina di Frigole included) and entrusted Franco Cannaviello with the task of studying their nature to enhance them. Cannaviello concluded that the Acquatina di Frigole lagoon should be connected to the sea through a mouth. Finally, he argued that the lagoon thus built could have been an excellent fishing reserve. The failures of mechanical drying, the impossibility of filling the swamp due to the enormous quantities of materials needed and, on the other hand, the prospect of creating a less suitable environment for proliferation of mosquitoes through the salting of the marsh environment, in addition to the possibility of having an economic advantage from the use of the lagoon as a reserve for fishing, convinced the ONC technicians to pursue this idea. . On the right side of the map, the path designed for the Giammatteo River is visible. Originally the river consisted of three branches (here evidenced with blue lines), gathered in the area called "la tunda", which ended directly in the Acquatina di Frigole lagoon. The project instead provided that the mouth was subject to a canalization that went around the Acquatina di Frigole lagoon and ended at sea south of the Torre Chianca.
Tree species in the surrounding areas were selected based upon their capacity to absorb the remaining water and facilitate soil cultivation. This reclamation system actually turned out to be ineffective because the channels intersected the surficial aquifer, so that, when the dewatering machines stopped working, the water table returned quickly to the initial level. In the early 1920s, therefore, the landscape was still characterized by extensive marshlands, and malaria was fairly widespread [125,126]; even the attempt to eradicate the disease by sending into the Acquatina water thousands of Gambusia affinis (Baird & Girard (1853)), an exotic species from America that had the characteristic of feeding on mosquito larvae, failed [124]. In 1921, the Opera Nazionale Combattenti (ONC) undertook the management of coastal areas (Acquatina di Frigole included) and entrusted Franco Cannaviello with the task of studying their nature to enhance them. Cannaviello concluded that the Acquatina di Frigole lagoon should be connected to the sea through a mouth. Finally, he argued that the lagoon thus built could have been an excellent fishing reserve. The failures of mechanical drying, the impossibility of filling the swamp due to the enormous quantities of materials needed and, on the other hand, the prospect of creating a less suitable environment for proliferation of mosquitoes through the salting of the marsh environment, in addition to the possibility of having an economic advantage from the use of the lagoon as a reserve for fishing, convinced the ONC technicians to pursue this idea.
In 1931 the project was therefore ready for the rehabilitation of the Acquatina swamp through the deepening of its central part, filling of the lateral sectors that were shaped with squared stones, connection of the large swamp with the small one through a canal and above all through the communication of the swamp with the sea through two outlets of appropriate width and depth. In 1936, thanks to the employment of over 450 workers a day, the reclamation work was completed: the present configuration was reached only at the end of World War II, with the arrangement of the Giammatteo River outlet. Today Giammatteo is characterized by two branches that converge near the province coastal road in a single channel, then flowing into the basin and to the sea (the final water supply . On the right side of the map, the path designed for the Giammatteo River is visible. Originally the river consisted of three branches (here evidenced with blue lines), gathered in the area called "la tunda", which ended directly in the Acquatina di Frigole lagoon. The project instead provided that the mouth was subject to a canalization that went around the Acquatina di Frigole lagoon and ended at sea south of the Torre Chianca.
In 1931 the project was therefore ready for the rehabilitation of the Acquatina swamp through the deepening of its central part, filling of the lateral sectors that were shaped with squared stones, connection of the large swamp with the small one through a canal and above all through the communication of the swamp with the sea through two outlets of appropriate width and depth. In 1936, thanks to the employment of over 450 workers a day, the reclamation work was completed: the present configuration was reached only at the end of World War II, with the arrangement of the Giammatteo River outlet. Today Giammatteo is characterized by two branches that converge near the province coastal road in a single channel, then flowing into the basin and to the sea (the final water supply can be regulated through a closed system of dams; Figure 4). The channel also constitutes the northern boundary of Acquatina. It is also clear that construction of the canal caused the interruption of the Acquatina water system, which was originally more extensive, including part of the areas located north of the Giammatteo river, nowadays buried. To highlight the above observations, it is possible to compare the topographic maps of Figures 3 and 5 (showing the undisturbed state of place) with that of Figure 6 (representing the situation after reclamation works). Today, the Acquatina di Frigole lagoon is bounded by man-made riverbanks mostly characterized by concrete banks and/or rock blocks for a linear extension of about 5628 m. The trend is sub-parallel to the coastline, while the basin area covers about 424.634 m 2 (Figure 2). highlight the above observations, it is possible to compare the topographic maps of Figures 3 and 5 (showing the undisturbed state of place) with that of Figure 6 (representing the situation after reclamation works). Today, the Acquatina di Frigole lagoon is bounded by man-made riverbanks mostly characterized by concrete banks and/or rock blocks for a linear extension of about 5628 m. The trend is sub-parallel to the coastline, while the basin area covers about 424.634 m 2 (Figure 2).

Hydro-Stratigraphy
The information provided by the exploratory holes that were drilled in geological investigations conducted in the last century (1950s and 1970s), compared with the geological surveys ( Figure 8) and the lithostratigraphic attribution by Bossio et al. [114], allowing for the definition of the hydrostratigraphic framework of the area. According to Cotecchia [88], the groundwwater movement is complex, owing to presence of two

Hydro-Stratigraphy
The information provided by the exploratory holes that were drilled in geological investigations conducted in the last century (1950s and 1970s), compared with the ge-ological surveys (Figure 8) and the lithostratigraphic attribution by Bossio et al. [114], allowing for the definition of the hydrostratigraphic framework of the area. According to Cotecchia [88], the groundwwater movement is complex, owing to presence of two separated aquifer systems: the deeper is in the Cretaceous limestones, and the other in the permeable post-Cretaceous rocks. Cretaceous rocks are intensely fractured and affected by karst phenomena, with high permeability (10 −2 m/s −10 −3 m/s) [88]. The top of these rocks tends to run to depth toward the coast (from −50 m to −107 m below ground level; see boreholes W1/RF/F and W4RF/F in Figures 8 and 9).  Figure 8 is also shown.
The Giammatteo River originates south of the area of interest, where there are two sources from which it is fed ( Figure 6). Water flowing in the river therefore circulates from the karstified Cretaceous limestone bedrock (Figure 7). Being the top of the limestone below sea level, with the less permeable Pietra Leccese Formation (fine grained calcarenites of Lower Miocene age) overlying the Cretaceous bedrock, the aquifer circulates under pressure, confined by the Miocene sediments. The presence of discontinuity systems in the Miocene succession allows the local rise of groundwater from the karst aquifer, thus originating springs [83,90]. In their upwelling, the waters mix with others coming from the more surficial Miocene (the aquifer hosted in the Piromafo level)-Pliocene-Pleistocene aquifers, as well as with other sources present along the river.
The flow rate of the watercourse is about 1000 L/s, with salinity of 2.4 PSU, while salinity of the Acquatina di Frigole lagoon is about 25 PSU (Table 1). The survey of the 1879 cartography (Figure 9), at a scale of 1: 50,000, shows that once the canal only flowed into Acquatina, without any outlet to the sea (for detail see also Figure 3).
The bottom is characterized by 1-m-thick clayey sediments, forcing the Pliocene aquifer to circulate under pressure. In the middle portion of the basin, where the canal is present, removal of the clayey sediments allows the outcrop of the calcarenite deposits belonging to the Pliocene Uggiano la Chiesa Formation [67]. The Pliocene unit constitute a porous aquifer in which the impermeable layer is the compact limestone of Andrano Calcarenite (Upper Miocene). Between the two units, a breccia layer is present. In conclusion, the waters of the Acquatina di Frigole lagoon derive from the spring located at its southern rim; in addition, the basin receives a further supply of seawaters at its bottom, this being at a lower elevation below the average sea level, and from the communication canals with the sea (E side) and the Giammatteo River (from inland).  Figure 8 is also shown.
The Pietra Leccese Miocene sediments (M1 in Figure 8) overlay the Cretaceous rocks and crop out widely in the study area. It also includes layers of compact yellowish, finegrained calcarenites with decametric thickness [114]: these are described in the literature as "Piromafo" and are famous for the presence of glauconite, represented at the study area by greyish-greenish calcarenites with cavernous facies (Figure 9b,c). These layers host an aquifer, from some meters to 40 m thick, with groundwater velocities on the order of about 18m/day [88]. Compact calcarenites belonging to the Upper Miocene Andrano Calcarenite formation (M2 in Figure 5) overlie the Piromafo. Eventually, the Plio-Pleistocene calcarenites and calcirudites (P1 and P2 in Figure 8) onlap the Miocene rocks, outcropping along the coast and hosting a very shallow aquifer (Figure 9d). Their low permeability is mostly due to porosity, with minor effects of karst phenomena.
The Giammatteo River originates south of the area of interest, where there are two sources from which it is fed ( Figure 6). Water flowing in the river therefore circulates from the karstified Cretaceous limestone bedrock (Figure 7). Being the top of the limestone below sea level, with the less permeable Pietra Leccese Formation (fine grained calcarenites of Lower Miocene age) overlying the Cretaceous bedrock, the aquifer circulates under pressure, confined by the Miocene sediments. The presence of discontinuity systems in the Miocene succession allows the local rise of groundwater from the karst aquifer, thus originating springs [83,90]. In their upwelling, the waters mix with others coming from the more surficial Miocene (the aquifer hosted in the Piromafo level)-Pliocene-Pleistocene aquifers, as well as with other sources present along the river.  11 12 of 26 Figure 9. Stratigraphies in the Acquatina di Frigole area (data re-elaborated from the archive of Ente Irrigazione). Adapted from geological formations follows the work by Bossio et al. [114]. Borehole location is shown in Figure 8.  [114]. Borehole location is shown in Figure 8.
The flow rate of the watercourse is about 1000 L/s, with salinity of 2.4 PSU, while salinity of the Acquatina di Frigole lagoon is about 25 PSU (Table 1). The survey of the 1879 cartography (Figure 9), at a scale of 1: 50,000, shows that once the canal only flowed into Acquatina, without any outlet to the sea (for detail see also Figure 3). The bottom is characterized by 1-m-thick clayey sediments, forcing the Pliocene aquifer to circulate under pressure. In the middle portion of the basin, where the canal is present, removal of the clayey sediments allows the outcrop of the calcarenite deposits belonging to the Pliocene Uggiano la Chiesa Formation [67]. The Pliocene unit constitute a porous aquifer in which the impermeable layer is the compact limestone of Andrano Calcarenite (Upper Miocene). Between the two units, a breccia layer is present. In conclusion, the waters of the Acquatina di Frigole lagoon derive from the spring located at its southern rim; in addition, the basin receives a further supply of seawaters at its bottom, this being at a lower elevation below the average sea level, and from the communication canals with the sea (E side) and the Giammatteo River (from inland).

Ecology
The Acquatina di Frigole lagoon is a habitat included in a wide Site of Community Importance (SCI) and Special Area of Conservation (SAC) under the Habitat Directive 92/43/EEC, named "Aquatina di Frigole" (IT9150003) according to the NATURA 2000 network. It includes habitats with "priority" status in the Annex I of the Directive 92/43/EEC, such as 1120* Posidonia beds (Posidonion oceanicae), 1150* Coastal lagoons and 2250* Coastal dunes with Juniperus spp. These, in danger of disappearance, have a higher degree of protection compared to 'non-priority' habitats, the latter including 1210 Annual vegetation of drift lines, 1310 Salicornia and other annuals colonizing mud and sand, 1420 Mediterranean and thermo-Atlantic halophilous scrubs (Sarcocornetea fruticosi), 2120 Shifting dunes along the shoreline with Ammophila arenaria ('white dunes') and 2260 Cisto-Lavenduletalia dune sclerophyllous scrubs.
Aquatina di Frigole has also a high variability of plant species. Along the banks of the basin, the sea aster Aster tripollum, the common reeds Phragmites communis and Phragmites australis and the glasswort Arthrocnemum glaucum are very common. The Mediterranean maquis has shrub species such as the rock rose Cistus creticus, the narrow-leaved cistus Cistus monpelliensis and tree species such as the olive tree, the maritime pine and the holm oak. Other species present are the pistache Pistacia lentiscus, the myrtle Myrtus communis, the apulian ophrys Ophrys apulica, the milkworts Polygala major, the mock privet Phillyrea latifoglia, the flax-leaved daphne Daphne gnidium and the mallow-leaved bindweed Convolvolus althaeoides. Along the dune coast, it is possible to observe the sea spurge Euphorbia paralias, the cutandia grass Cutandia maritima and the sea lily Pancratium maritimum, which is one of the most beautiful plants of the sandy coasts. Very resistant to arid environments and sea salt, and for this reason often used to consolidate the coastal dunes, is the sally-my-handsome Carpobrotus acinaciformis, generally living in association with the sharp cedar Juniperus oxycedrum, the cottonweed Otanthus maritimus, the hairy thorny broom Cytisus infestus and the European beachgrass Ammophila littoralis. Among the species present in Aquatina di Frigole, there is also the pillwort included among the plant species of the National Red List. In addition, the variety of environments and habitats in the entire protected area allows a rich presence of numerous nesting and migratory birds. Some of these are listed in the Annex I of Birds Directive 2009/147/CE as vulnerable and at risk of extintion, such as the purple heron Ardea purpurea, the bittern Botaurus stellaris, the hen harrier Circus cyaneus, the little bittern Ixobrychus minutus, the White-eyed Pochard Aythya nyroca and the Black-winged Stilt Himantopus himantopus. Along the embankments, it is possible to come across in many other birds, including different types of egrets and rapaceous. Furthermore, the lagoon hosts an abundant and valuable ichthyofauna, different species of crustaceans and molluscs, including the endemic Mediterranean bivalve Pinna nobilis (listed in Annex IV of the Habitats directive, and considered an endangered species in the IUCN Red list) [127][128][129].

Sinkhole Evolution
The evolution of the Acquatina sinkholes has been examined starting from 2006, the year in which the first high-resolution aerial photographs date back ( Figure 10). The sinkhole process seems to have started in the central part of the basin, where the canal built for reclamation of the original marshland is present. In 2006 a high number of sinkholes was present along this channel, the highest frequency being observed exactly at the intersection with another orthogonal channel; relatively few sinkholes were recognizable in the remaining parts of the basin. Taking as a reference the northernmost portion of the basin, bounded by the two orthogonal channels and by the outer northeastern perimeter of the basin, we can observe how, in 2006, where the NE-SW channel is present, at least three sinkholes are recognizable; two of these (nos. 1 and 2 in the 2006 photo in Figure 10) are clearly outlined, with diameters of approximately 58 m (the sinkhole located to the east) and 56 m, respectively. Some additional small sinkholes are present in the northern portion of the basin, showing diameters of about ten meters.
The analysis of the 2008 aerial photos shows the sinkhole process in evolution: the two features previously recognized, in 2008, reached 62 m in diameter, whilst additional sinkholes have opened inside the basin (zone labelled with no. 3 in the 2006 photo). The sinkholes seem to be aligned in the NW-SE direction (the same as the basin elongation), the largest reaching a diameter of 20 m. In 2010, practically the entire portion of the canals is affected by sinking processes, which makes it difficult to discriminate among the individual sinkholes due to widespread coalescing processes. Within the basin, too, the sinkholes have grown in number (always according to the aforementioned direction) and size (the largest are about 30 m in diameter). The same trend can be further appreciated two years later, in the 2012 photos, with the sinkholes of less recent formation that have reached 40 m of diameter while some others begin to merge. In 2016 the sinkholes are widely coalescing, the diameter of the largest ones reaching 50 m. Eventually, the 2018 photos show that almost 80% of the surface of the basin is affected by sinking processes. The survey carried out in February 2019 with the UAV DJI Phantom 4 pro, equipped with a 1-inch, 20-megapixel RGB camera, allowed us to prove that the sinkhole had reached, at that time, a diameter of 54.77 m. The sinkhole enlargement rate can be estimated at about 5 m/year, with a maximum subsidence of about 0.7 m (Figures 11 and 12). reached 40 m of diameter while some others begin to merge. In 2016 the sinkholes are widely coalescing, the diameter of the largest ones reaching 50 m. Eventually, the 2018 photos show that almost 80% of the surface of the basin is affected by sinking processes. The survey carried out in February 2019 with the UAV DJI Phantom 4 pro, equipped with a 1-inch, 20-megapixel RGB camera, allowed us to prove that the sinkhole had reached, at that time, a diameter of 54,77 m. The sinkhole enlargement rate can be estimated at about 5 m/year, with a maximum subsidence of about 0.7 m (Figures 11 and 12).  The substrate of the lagoon hosts the seagrass meadows Cymodocea nodosa, which ap pear to surround most of the sinkholes (Figure 13). This phanerogam form in the lagoon' extensive and dense meadows equivalent to those formed by others marine phanerogams In particular, the meadows made up of this plant, even if they are not equivalent to thos The substrate of the lagoon hosts the seagrass meadows Cymodocea nodosa, which appear to surround most of the sinkholes (Figure 13). This phanerogam form in the lagoon's extensive and dense meadows equivalent to those formed by others marine phanerogams. In particular, the meadows made up of this plant, even if they are not equivalent to those of Posidonia oceanica, provide an environment for the reproduction and development of even typical marine organisms. It lives either along the coasts in the hypersaline environments and in shallow water such as the lagoons [130]. The characteristics of this plant make it an excellent pioneer marine plant, capable, if conditions suitable for the survival of the plants on a seabed are restored, to colonize over time large underwater areas. The same dense seagrass meadows, mainly Cymodocea nodosa, cover the seafloor of the continental shelf of the Maltese islands in the shallower waters, reaching a maximum depth of ca. −55 m. The seagrass meadows colonized coarse-grained sediment and bedrock across parts of the seafloor off-shore NE Gozo, Comino to Wied Pwales and SE Malta [131]. The Maltese archipelago including Malta, Gozo and Comino is one of the few emergent areas of the Pelagian Platform consisting of thick exposures of Mesozoic shallow water carbonate sequences and volcanic deposits [131]. As observed in other areas worldwide [132][133][134][135][136], the vegetation colonizing specific karst landforms may provide useful information about the chemical and physical parameters of the local environment. The substrate of the lagoon hosts the seagrass meadows Cymodocea nodosa, w pear to surround most of the sinkholes (Figure 13). This phanerogam form in the extensive and dense meadows equivalent to those formed by others marine phane In particular, the meadows made up of this plant, even if they are not equivalent of Posidonia oceanica, provide an environment for the reproduction and develop even typical marine organisms. It lives either along the coasts in the hypersaline ments and in shallow water such as the lagoons [130]. The characteristics of t make it an excellent pioneer marine plant, capable, if conditions suitable for the of the plants on a seabed are restored, to colonize over time large underwater a same dense seagrass meadows, mainly Cymodocea nodosa, cover the seafloor of t nental shelf of the Maltese islands in the shallower waters, reaching a maximum ca. −55 m. The seagrass meadows colonized coarse-grained sediment and bedro parts of the seafloor off-shore NE Gozo, Comino to Wied Pwales and SE Malta [ Maltese archipelago including Malta, Gozo and Comino is one of the few emerg of the Pelagian Platform consisting of thick exposures of Mesozoic shallow w bonate sequences and volcanic deposits [131]. As observed in other areas worldw 136], the vegetation colonizing specific karst landforms may provide useful info about the chemical and physical parameters of the local environment.

Discussion
The development of sinkholes along the main tectonic trends has been documented in many karst areas worldwide [68,[137][138][139][140][141], thus testifying to the preminent role played by the main discontinuity systems in favouring development of karst conduits, and the consequent groundwater flow in karst aquifers along such features [142][143][144][145]. Even at the surface, without producing real sinkholes and dramatic landforms at the ground, doline occurrence is often linked to the main structural lineations in the carbonate rock mass [10,[146][147][148]. As regards Apulian karsts, here, too, several locations have demonstrated that the alignment of the sinkhole and doline features is highly controlled by the most widespread discontinuity systems. This was true in Salento, both in the inland areas [69,75,149] and at several coastlines, as in the case of Casalabate, Alliste and Torre Castiglione [37,45,46,150].
Focusing on the study area dealt with in this article, it is evident that the works for the construction of the canals at Acquatina di Frigole have weakened and thinned the layers of calcarenite rock that constituted the vault of cavities within the Mio-Pliocene sediments, generated by hyperkarst processes due to the mixing of fresh and seawaters and the resulting stronger aggressiveness of dissolution processes [47][48][49]. Upward stoping of the cavities initially caused the collapse of the vaults where these were less thick (this mostly occurred in correspondence of the canals), and where the rock mass was strongly fractured, probably also as a consequence of the excavation works. These collapses favoured the progressive enlargement of the cavities, even in the inner portions of the basin, along NW-SE oriented tectonic lines, likely associated with the axis of the synclinal fold in which the whole original Acquatina lagoon developed. Based upon the available data and the existing sets of photographs, the sinkhole enlargement rate (i.e., the increase in width of sinkholes) can be estimated at about 5 m per year. As concerns the typology of these karst landforms [2,3,151], the Acquatina sinkholes belong to the class of suffusion sinkholes, related to the undermining of the cover deposits by internal erosion (Figure 14). In detail, suffusion sinkholes develop where the cover behaves as a ductile or loose granular material, settling gradually without the formation of significant failure planes [2]. Typically, funnelor bowl-shaped landforms are produced, with the classical circular form in plan [10,152] and a diameter in the range from less than 1 m to a few meters. Suffusion sinkholes differ from the other typology of features produced by the undermining of the cover deposits by internal erosion, which is cover collapse sinkhole: in this case, the cover deposits respond with brittle behaviour from a rheological standpoint, generating the upward migration of an arched cavity [1,2,[153][154][155]. The two categories of suffusion sinkholes and cover collapse sinkholes are the most sensitive to human alterations and present the highest probability of occurrence.
In the Acquatina di Frigole case study, the loose sandy silt cover deposits moved down along the main discontinuity systems, to fill the cavities generated within the underlying Mio-Pliocene calcarenites. The contemporary upwelling of freshwater, combined with the sink in the central part of the depressions is not favourable to the establishment of Cymodocia nodosa, which, on the other hand, tends to develop and fully grow around the newly formed sinkholes. In this way, the growth and spreading of Cymodocia nodosa make the identification of the sinkhole rims much easier, marked by development of the seagrass. Figure 14. Sketch of the sinkhole evolution (not to scale). Please note that the first sinkholes developed in correspondence of the two artificial canals, probably because of the reduced thickness of the recent sands. Phase one: sands move down into the voids, which are progressively enlarged by the joints, thus forming small depressions at the surface. Rising brackish water through the joints favours plants to take root; however, continuous settling of sands pushes them at the rims of the depressions. Phase two: both dissolution and sand infilling go on, and wider depressions are originated due to coalescing sinkholes. Phase three: continuing infilling determines a general lowering of the basin bottom.

Conclusions and Future Perspectives
Sinkhole development in coastal areas has a significant impact on human activities, but, at the same time, is in some way interlinked with anthropogenic actions. Coastal areas are always zones of high economic interest due to presence of infrastructures (harbours, seafood farming, industrial activity, etc.) and to the relevance for tourist economies. Any process affecting the coast therefore represents a threaten to the local economy, with particular regard to gelogical hazards, and is worth being fully studied in order to develop the most proper actions to reduce the risk. In the case study presented here, as demonstrated by the formation and evolution of several sinkholes in a coastal marshland of southern Italy, it is highly likely that, in the near future, the Acquatina di Frigole lagoon could be further characterised by the enlargement of the documented sinkholes and/or the formation of new ones. This is clearly indicated by the high enlargement rate, showing an increase in width on the order of about 5 m/year, with maximum subsidence of about 0.7 m. It is worth noting that there are not many documentations about the evolution rate of sinkholes, either in Apulia or in other karst areas worldwide (see in this regard the review in [2]). Even though many other sites affected by sinkholes are present along the Apulian coastlines, Acquatina di Frigole is of significant relevance since within the marsh area, the environment can be considered as natural after the realization of the basin and of the canals. This makes the site a wonderful laboratory to evaluate the sinkhole evolution, also in terms of their interaction with vegetable species within the marshes and with their growth in relation with the local chemical and physical conditions. It is therefore crucial to continue monitoring the site by means of periodic surveys by drones, which could be extremely useful to detect changes in sinkhole size and to measure possible changes in the rates of formation and evolution, and ROV and subbottom profilers, useful to better define the basin bathymetry, the morphometric features of sinkholes and to recognize the top of the calcarenite bedrock below the sandy silts. Similarly, it should be relevant to integrate the presence and the evolution of the sinkholes in the Acquatina lagoon in relation to the functional processes such as the decomposition of the seagrass litter Cymodocea nodosa, as well the variation of the body size structures of the benthic macroinvertebrates in the vicinity of these structures [156][157][158][159]. The observation of these phenomena in the protected area of Acquatina di Frigole could help to predict land movement in urbanized areas and to prevent potential damage to roads and house.
Another aspect worth consideration is that of geotourism [22,23], that is, establishing pathways and organizing sites for valorisation through a naturalistic tourism aimed at favouring the conservation of the natural landscape and at allowing people to understand, from an onsite visit, the beauty of the landforms while also gaining scientifically sound information about their genesis. In Apulia, with karst as the main geomorphological agent working in the development of the local landforms, karst geosites are increasingly gaining attention, both at the surface and in the underground world as well [21,25,30]. Given the high tourist vocation of the region, this growing importance of karst geotourism in Apulia, as well as in Salento, planning a guided tour at Acquatina di Frigole and the surroundings coastal areas might be a good opportunity for valorisation and preservation of these marshlands, and to explain the sinkhole processes and their evolution in relation with man-made structures.