The general characteristics of the water masses and their circulation in the western Mediterranean have been well described in previous works (e.g. Font et al. 1988). Low-salinity Atlantic Waters (AW) inflows at surface through the Strait of Gibraltar following a cyclonic path in the western Mediterranean. These recently arrived AW (rAW) reaches the Balearic Islands and the Strait of Sicily in a few months. Then, it flows towards the north to the Tyrrhenian and Ligurian seas, reaching the northern slope, and continues towards the south, affecting the Catalano-Balearic Sea and closing a cyclonic circuit in the NW Mediterranean basin (Millot 1990). The AW becomes progressively modified along this pathway under the effect of vertical mixing and evaporation processes that act mainly during the winter season. In addition, along the northern slope, AW incorporates freshwater inputs from rivers that help to maintain lower salinity inshore, but further offshore it becomes saltier as it remains in the central open-sea part of the Catalano-Balearic Sea. This old AWs (oAW) is separated from the coastal rAW by a marked shelf-slope density front (Salat and Font 1987, Font et al. 1988).

Along the shelf and slope and in the open sea of the northwestern Mediterranean, wintertime heat loss, vertical convection and mixing typically affects the upper layer occupied by oAW, forming an intermediate layer characterized by a relative minimum temperature (Lacombe and Tchernia 1972, Salat and Font 1987) and currently known as Western Mediterranean Intermediate Water (WIW). These waters typically spread towards the SW, and their signature just below the AW is progressively eroded in summer and autumn. Levantine Intermediate Water (LIW), which originates in the Levantine basin, in the eastern Mediterranean, flows into the northwestern Mediterranean below the WIW, also following a cyclonic path in the western Mediterranean. LIW usually has both temperature and salinity maxima centred around 400-600 m depth (Font 1987, Millot 2013). Deeper, the water column is occupied by Western Mediterranean Deep Water (WMDW), which can be identified by relative minima of both potential temperature and salinity (Table 1).

The dynamics of the NW Mediterranean Sea is driven by the seasonal cycle. As noted above, the water masses are modified in the course of the year by the ocean/atmosphere interaction. Surface temperature varies seasonally by more than 14°C (Salat et al. 2002). A seasonal thermocline develops from early spring to late autumn, whereas in winter the water column homogenizes down to different depths, depending on wind strength, air temperature, surface salinity and marine circulation. In the northwestern Mediterranean open-sea winter heat losses and evaporation caused by cold, dry northerly wind episodes cause a completely homogeneous water column down to the bottom. This is a well-known region for open-sea deep convection (MEDOC Group 1970), which produces new deep water (WMDW) that can occur on a yearly basis (Somot et al. 2016). On the continental shelf of the Gulf of Lions, these winds can also induce the cooling and evaporation of coastal waters, which are initially less saline but become colder and denser, sinking and travelling over the bottom of the shelf and cascading down the continental slope, mainly through submarine canyons, until they reach their equilibrium depth (Millot 1990, Durrieu de Madron et al. 2005). In the initial stages of the cascading process, dense waters spread around the shelf break depth (150-200 m) and contribute to the formation of WIW (Fieux 1974, Dufau-Julliand et al. 2004). In extremely cold and dry winters, dense shelf waters can cascade to deeper levels, sometimes mixing with the waters present, namely the warmer and saltier LIW layer and the underlying WMDW (Salat et al. 2006, Font et al. 2007, Puig et al. 2013) to reach the bottom, and also contributing to the renewal of the WMDW.

Salat et al. (2002) reported on the way in which the seasonality of the water column stratification and the riverine inputs affect the hydrographic structure and the distribution of nutrients, chlorophyll and suspended matter on the Ebro shelf (NW Mediterranean). These seasonal cycles should be superimposed on long-term decadal trends such as the progressive increase in temperature and salinity that has been detected in surface waters of the western Mediterranean during the past few decades (Krahmann and Schott 1998, Salat and Pascual 2002, 2006, Vargas-Yáñez et al. 2005). The initial trends reported by Vargas-Yáñez et al. (2008) for the first half of the 20th century accelerated after the mid-century (Rholing and Bryden 1992, Tsimplis and Baker 2000). An overall warming trend of around +0.02°C to 0.03°C yr^–1 recorded in coastal areas for the period 1974-2005 showed a sharp reduction in the warming rates during the 1990s, suggesting that Mediterranean warming is superimposed on decadal oscillations (Vargas-Yáñez et al. 2008).

The city of Barcelona (ca. 2 million inhabitants plus an increasing tourist population reaching an average of several million visits per year) is located in the northwestern Mediterranean, on the Catalan coast (Fig. 1). It is a micro-tidal zone with a typical range of about 0.2 m, in which waves are the main stirring mechanism controlling coastline evolution (Ojeda and Guillén 2008). The most energetic storms approach from the east, have a typical duration of a few days, and are often associated with meteorological cyclonic activity in the western Mediterranean (Ojeda and Guillén 2008). The city is flanked by two small rivers, the Besòs in the north and the Llobregat in the south, and several storm sewers discharge freshwater to the coastal area during rainfall periods (Fig. 1). An important commercial harbour is located on the left side of the Llobregat River mouth. To the north, along the city seafront there are three marinas and more than 3 km of beaches before the Besòs River mouth is reached.

The hydrography of Barcelona coastal waters is characterized by strong seasonality, with obvious major anthropogenic influences (Romero et al. 2014). However, seasonal variability also includes natural variability of inorganic nutrients and phytoplankton. In general, observed nutrient concentrations are highest in winter and lowest in summer (Arin et al. 2013), since the main mechanisms of fertilization of the coastal water masses are linked to both the disruption of the thermocline and the occurrence of freshwater inputs, associated either with the rivers or with the storm sewers. Phytoplankton biomass shows a main peak in winter/early spring and often a secondary peak in autumn (Arin et al. 2013). Interannual changes in phytoplankton composition related to nutrient inputs associated with oceanic water intrusions have been reported (Arin et al. 2013).

The present work is based on the time series of oceanographic data routinely collected off Barcelona city as part of the activities of the Coastal Ocean Observatory (COO) of the Institute of Marine Sciences (ICM-CSIC) of Barcelona. The COO was created in 2001 to analyse land-sea interactions under the perspective of the impact of large cities on the marine environment, providing complementary information to existing monitoring programmes. The COO aims to conduct physical, morphological and biological monitoring with the highest feasible resolution and a long-term perspective in order to determine the behaviour and evolution of a coastal system where natural and human influences coexist.

The data used in this study were obtained from 117 monthly hydrographic surveys carried out between April 2002 and November 2012, with a mean periodicity of 33 days (maximum 94 days, minimum 11 days). The surveys were carried out using the small boat Itxasbide, which is 7.6 m long. Each survey consisted of eight CTD casts using an SBE 25 CTD coupled with turbidity and fluorescence sensors. Casts were distributed along two transects 2.5 km apart across the inner continental shelf. Each transect comprised four stations at water depths of 10, 20, 30 and 40 m water depth (hereafter, respectively, stations 1-1, 1-2, 1-3 and 1-4 for transect 1 and 2-1, 2-2, 2-3 and 2-4 for transect 2) (Fig. 1). Surface and bottom samples for laboratory measurements of salinity, turbidity and chlorophyll a were taken with a bucket (between 0 and 0.5 m depth) and with a Niskin bottle (1.5 m above the bottom), respectively.

CTD raw data were processed with the SBE data processing software (SEASOFT – Win32) to obtain the hydrographical variables of the water column (conductivity, temperature and depth) every 0.5 m. TEOS-10 hydrographic variables (temperature, salinity and density) were calculated following the Gibbs Seawater Oceanographic Toolbox (IOC et al. 2010). Time was set to GMT.

During the study period, two different SBE 25 CTD probes were used (SN 97 and 104). The SN 97 CTD, used from April 2002 to August 2007, was calibrated in February 2002, May 2003 and February 2005. The SN 104 CTD, used thereafter, was calibrated in March 2002, August 2007 and August 2008. The salinity of water samples for routine CTD data control was analysed using a Guildline Autosal 8400B laboratory salinometer. Discrepancies in salinity measurements were small (mean difference, 0.08; relationship, Y=0.998 X; N=605 samples; R²= 0.99).

Turbidity was measured by a 25-cm Sea Tech transmissometer (SN 418) (based on light attenuation) during the first 23 surveys, and two Seapoint turbidimeters (SN 10250 and 102666) (based on light scattering) thereafter. Water samples were filtered through polycarbonate filters to determine suspended particulate matter concentration (mg L^–1). The turbidity measurements were calibrated against the suspended sediment concentration (SSC) by means of a linear regression. A specific calibration was performed for each sensor-CTD set (N= 430; R²=0.55, 0.72, 0.69; 0.16 for the different calibrations).

Fluorescence was measured by Sea Tech Fluorometers (Seapoint Chlorophyll Fluorometers) SN 228 and 2205, and a WETLabs WETStar Fluorometer (SN 2089). The fluorescence measurements from the bottom water samples were correlated against chlorophyll a concentrations (as an indicator of phytoplankton biomass). Data from surface waters (<0.5 m water depth) were discarded due to a possible phytoplankton photoinhibition (light induced decrease in fluorescence) that biases the chlorophyll a–fluorescence correlation (Estrada 1996). For chlorophyll a analysis, water samples (100 mL) were filtered through Whatman GF/F fibre filters, which were then kept frozen. Chlorophyll a was extracted in 90% acetone for approximately 24 h in the dark and at 4°C, and the fluorescence of the extract was measured with a Turner Designs fluorometer (Yentsch and Menzel 1963). Five linear regressions between fluorescence and chlorophyll a were established according to the different fluorescence sensors and CTD configurations (total number of samples, 773; N=48 to 345; R²=0.41, 0.55, 0.55, 0.64 and 0.81). The resulting expressions were used to calibrate the fluorescence data as µg L^–1 of chlorophyll a.

Several pluvial outflows discharge in the coastal area of Barcelona city during rainfall periods and, before analysing the results, we were not confident about the similarity between the two hydrographic transects. However, data obtained in transects 1 and 2 were very similar. For example, the comparison between the mean values of variables obtained from the deepest CTD profiles (stations 1.4 and 2.4) revealed highly correlated temperature, salinity, density and SSC (R²>0.97) during the whole study period. Therefore, to illustrate the oceanographic conditions found and to avoid reiteration, only data obtained in transect 1 are shown in this paper.

Within the study period, during summer 2009 and from February to May 2011, we had the opportunity to investigate the short-term variability of surface water temperature through a temperature sensor integrated in an AQUAlogger 210TYT probe moored at the position of the CTD at station 1.1 (Fig. 1), where a harbour approach navigation post light is located. Measurements were obtained every 30 minutes in subsurface waters (1.5 m below surface water level).

Monthly meteorological information (mean air temperature and accumulated rainfall) and wave climate (accumulated hours of storm waves) in Barcelona during the study period were provided by the Observatori Fabra (http://www.fabra.cat/meteo/) and Puertos del Estado (http://www.puertos.es/es-es/oceanografia/), respectively.

Detailed seawater temperature observations in spring 2011 measured at the harbour approach navigation post light (station 1.1) revealed a strong diel variability in shallow waters (Fig. 2). The diel temperature variation associated with the cycle of solar heating was about 0.5°C to 1°C in surface waters (1.5 m below the surface). The maximum diel temperature variation reached almost 2°C. The coldest water typically occurred in the early morning, not later than 7:00 h, and the warmest in late afternoon, around 17:00-18:00 h. Diel temperature variability was lower at 10 m water depth (usually lower than 0.5°C) and showed a similar pattern (data not shown). Seasonal temperature variations such as the strong increasing gradients in spring were superposed on diel oscillations. For instance, the surface temperature increased at an average rate of 0.09°C day^–1 from March to June 2011 (Fig. 2). Strong winds and wave storm events can also induce temperature changes, such as the one occurring in late May 2011, which mask the diel cycle caused by solar heating.

High-frequency temperature data were also used to assess possible biases in the routine sampling, since CTD measurements were always carried out between 8:00 and 13:00 h. According to the observed diel cycles in spring and summer, the measured water temperatures could be expected to be (on average) slightly colder than the mean daily temperature, at least during these seasons. Consequently, the representativeness of the monthly data used in this work can only be considered within the perspective of a long-term series, in which mean monthly values can be derived from a single measurement.

The monthly air temperature ranged between 6°C and 28°C. The warmest months were August 2003 and July 2006, and the highest annual mean was recorded in 2006. The coldest months were February and December 2005 and January 2010, and the lowest annual mean was in 2010. The mean annual cycle shows that the warmest period was June-August and the coldest December-February (Fig. 3).

The annual rainfall ranged between 450 and 950 mm. It was above 700 mm in 2002, 2010 and 2011 and below 600 mm in the remaining years. The mean monthly rainfall during the study period ranged between 31 and 101 mm. The driest period within the mean annual cycle was from June to August and the maximum mean rainfall occurred in October (Fig. 3).

Storm waves also displayed strong seasonality, as illustrated by the accumulated hours of significant wave height (Hs) higher than 2 m (Fig. 3), which is representative of the major storms for this area (Ojeda and Guillén 2008). Most of the storms occurred during the period from October to April, which is characterized by more than 10 hours per month of high-wave activity. The period from May to September was hardly affected by high waves. The total annual time of storm waves ranged between 80 and 289 hours/year in 2005 and 2003, respectively (Fig. 3).

No interannual trends in air temperature, rainfall and waves were observed during the period 2002-2012 (Fig. 3).

Temperature, salinity and water density displayed interannual changes with no obvious long-term trend (Figs 5 and 6). Yearly averaged values of these variables within the study period show a maximum temperature in 2006 and salinity and density maxima in 2005 (Fig. 10). Minimum annual temperatures occurred in 2004 and 2010, minimum salinity in 2011 and minimum density in 2008. Data from 2002 were not considered because of the lack of data in January-March 2002.

In order to better identify potential temporal trends, the slope of the linear regression fitting was calculated. The values of the slope, the 95% confidence interval and the p-values are displayed in Table 3. Since the p-values are clearly above 0.05 (except for SSC and chlorophyll a), it can be concluded that temperature, salinity and density data showed no significant increasing (or decreasing) trend, while chlorophyll a and SSC showed a small but significant decreasing trend.

Seawater properties in the Barcelona coastal area display the characteristic seasonal cycle of the coastal waters of the NW Mediterranean (Salat et al. 2002). The warming period starts in March-April with a progressive stratification, reaching a maximum surface temperature in August. Then, surface cooling and wind-driven vertical mixing in the autumn (late October-November) break the seasonal thermocline, leading to vertical homogenization. Cooling of the whole water column by convection and vertical mixing continues during the winter (December to February) until the start of the next warming cycle in March (Figs 5 and 8). The salinity pattern is characteristic of areas where freshwater inputs are scarce enough to be able to generate significant changes in the salinity of the coastal waters. However, strong winds in winter also favour vertical mixing and evaporation, causing an increase in salinity (Figs 4, 5 and 6). The seasonal cycle of surface chlorophyll a concentration is typical of the Mediterranean coast (Siokou-Frangou 2010, Nunes et al. 2018). However, integrated values at the deep station display a different seasonal pattern because they include the contribution of near-bottom layers of high chlorophyll a, a feature that has been associated with enhanced nutrient availability (Guallar and Flos 2017).

The absence of interannual trends in time series of temperature, salinity and density in Barcelona during the period 2002-2012 is consistent with observations of meteorological variables and seawater temperature in different Mediterranean areas. For instance, the mean monthly air temperature in Barcelona city displayed a seasonal oscillation with earlier peaks (1-2 months before) and greater variability than depth-averaged seawater temperature, but no long-term trend was observed (Fig. 11). Additionally, the comparison between Barcelona time series and the averaged water temperature (0-35 m water depth) measured at L’Estartit station [located about 150 km north of Barcelona, see Salat and Pascual (2002) for a detailed explanation of methods and results at this coastal station] showed that the two series followed the same seasonal pattern had similar absolute values and displayed no long-term trends during the study period (Fig. 11). Although a long-term water warming was described from the whole 40-year time series at L’Estartit by Vargas-Yáñez et al. (2008, 2010), this trend is much less clear if only the 20-year period (1991-2011) is taken into account. As pointed out by these authors, warming trends are neither linear nor constant processes, and oscillations of different periods can be superimposed on the general trend, producing an apparent hiatus. Therefore, no significant temporal trends in water temperature, salinity and density were detected in the coastal waters off Barcelona in the period 2002-2012, one possible reason being that 11 years is too short a time span to detect long-term trends.

The significant interannual (decreasing) trends of SSC and chlorophyll a should be interpreted with caution, because mean SSC and chlorophyll a values are low, indicating very restricted sedimentary inputs in coastal waters from rivers and city outfalls as well as general oligotrophic conditions. SSC time series show values lower than 5 mg L^-1 except for some water levels near the bottom and the surface during the period March to June 2004 (Fig. 5). Chlorophyll a concentrations in the time series samples show a maximum sample value of 9.3 μg L^-1, but typically remain below 1 μg L^-1. In addition, these mean low concentrations make the results very sensitive to the sensor properties and calibration equations. It must be taken into account, in this context, that both turbidity and fluorescence were measured using different sensors during the observation period (see methods). Therefore, although the decreasing trends of SSC and chlorophyll a were statistically significant, they could have been affected by errors and imprecisions in calibrations associated with the change of sensors in the period 2002-2012. Other potential forcing factors such as river discharges (and associated nutrient discharges), rainfall and wave climate displayed no interannual trend during the study period (Fig. 3), but one possible source of variability that cannot be excluded is the effect of water treatment plants that clean waste waters of the Barcelona city area, since the largest plants are located at both sides of the study area, near the Llobregat and Besòs rivers (Fig. 1) and they were expanded and improved in 2003 and 2005, respectively.

The highest mean daily air temperatures in the study period were measured in July and August 2003 (31°C and 33°C, respectively). In fact, five of the ten daily maximum temperatures recorded in Barcelona city during the whole last century (1914-2013) occurred in August 2003 (http://www.fabra.cat/meteo/). The heat wave of summer 2006 was also characterized in Barcelona by the maintenance of high temperatures during a long period (September-December 2006). This finding is consistent with the description of the heat wave of 2006 in Europe, which was due not only to the high air temperature in summer but also to the milder than usual temperature during the period September 2006 to February 2007 (Luterbacher et al. 2007).

The seawater temperatures recorded in Barcelona during the heat episodes of 2003 and 2006 were quite similar, although the warmest month of our series was August 2003 (Figs 6 and 12) and the warmest year 2006 (Fig. 10). The highest seawater temperature was also recorded in August 2003 (26.21°C at 2.5 m water depth), although extreme temperatures higher than 25°C were present in the shallower records of the water column in 6 of the 11 summers (2003, 2005, 2006, 2008, 2009 and 2010), suggesting that the presence of very warm coastal waters is quite usual during the summer period. Interestingly, the minimum and maximum depth-averaged seawater temperatures recorded at station 1.4 (40 m depth) were in the same year, making the strongest temperature contrast of the study period between 11.73°C and 22.83°C, in March and August 2003, respectively. The winter heat loss that produces extreme cold water episodes on the continental shelf is mainly caused by cold and dry northerly winds, which are enhanced by an anticyclonic anomaly in the North Atlantic and a cyclonic anomaly over the Baltic Sea that favours strong, cold, and dry winds in this area (Durrieu de Madron et al. 2013). The extreme heat wave in 2003 was caused by the northward shift of the polar jet, which allowed the anticyclone to expand over central Europe (Feudale and Shukla 2011). However, there is no obvious relation between cold and warm events.

Marine heat waves are usually defined on the basis of threshold temperatures (typically 90th percentile) extracted from time series at a specific site for a minimum length (typically 3-5 days) (Hobday et al. 2016, Schlegel et al. 2017). Consequently, the frequency and duration of the Barcelona time series would make it difficult to identify most of these episodes. To check the possibility of identifying the most extreme events during the study period we estimated de 2^nd and 98^th percentiles of temperature at 5 and 20 m water depth. Threshold temperatures were 11.99/11.99°C and 25.29/22.88°C at 5/20 m water depth, respectively. Cold water episodes occurred at 5 and 20 m water depth in March 2003, March 2010 and February 2012 and were identified simultaneously along the water column. The occurrence of marine heat waves based on these criteria would depend on the selected water depth. Warm episodes were identified at 5 m water depth in August 2003, July 2005 and September 2006. By contrast, warm episodes at 20 m depth were identified in September 2008 and August and September 2010. The different behaviour between cold and heat events is due to the homogeneity of the water column in winter and its strong stratification in summer. The maximum temperatures in surface waters are directly caused by radiation and atmospheric heat flux in July-August, whereas the maximum temperatures at 20 m water depth occur later (September), as a consequence of deepening of the upper mixed layer caused by surface heat loss and/or wind/wave–induced mixing (Fig. 8). This different timing in the maximum temperature along the water column should be taken into account in the evaluation of potential impacts of marine wave heats on the biological communities.

Coma et al. (2009) suggested a seawater temperature threshold of 18°C at 20 m depth as a good indicator of marine "summer conditions” at L’Estartit coastal station, because during the 40-year time series available there it was a value above which the thermocline was not broken by any perturbation. This means that when this temperature is reached at 20 m depth, stratification is consolidated and remains until the end of summer. To illustrate the application of this observation to Barcelona waters, we compared the temperature at 20 m water depth of station 1.4 and the stratification of the water column, represented by the standard deviation of the density profile (the Brunt-Väisälä frequency was also checked but it did not really add any information to the general description of temporal variability of the stratification and mixing) (Fig. 13). In general, the highest temperatures corresponded to high standard deviation in the 40-m water column, but the relation between the two variables was far from linear, especially at the beginning and the end of the stratification period. In some years, there was a strong stratification in May-June but the isocline of 18°C was shallower than 20 m. Conversely, in September-October the thermocline was deeper than the 40-m water column of our control profile, and the stratification of shallower waters was low (but the temperature was very high).

In spite of these uncertainties, we applied the criterion regarding water stratification proposed by Coma et al. (2009) to L’Estartit data as a simple tool for measuring the duration of the ”summer” conditions mentioned above. Following this criterion, the permanent stratification of the water column at L’Estartit occurred between 99 and 174 days per year during the study period. This well-developed stratification had a duration of 122 and 152 days in 2003 and 2006, respectively. However, the maximum persistence of water temperatures higher than 23°C at 20 m depth at L’Estartit station (45 days during the study period) matched with the warmest years (15 days in summer 2003 and 20 days in summer 2006) (Fig. 14). Although a direct relation between increased sea surface temperature (coupled with decreased rainfall and wind) and an extended stratification period, with implications for the definition of future climate change scenarios, has been described (Calvo et al. 2011), this was not observed in the analysed data. This would suggest that, in addition of the seasonal heating by radiation, the freshwater inputs and the intensity of mixing processes driven by waves, winds or oceanic circulation conditions should be taken into account for understanding the processes involved in the onset and overturn of stratification periods (Cheng et al. 2010, Magee and Wu 2017).

Therefore, seawater temperatures during the 2003 and 2006 summers show no obvious differences that could explain why a negative impact on the benthic ecosystem of the western Mediterranean occurred only in summer 2003 (Garrabou et al. 2009). As pointed out by Coma et al. (2009), the combination of extremely high temperatures and a long duration of the stratified period was probably what caused the mortality event of 2003, because higher temperature accelerated the metabolism, and stratification limited the availability of food. The main singularities of the year 2003 were the persistence of extreme seawater temperatures, the contrast between the coldest water in March and the warmest in August, and the strong storm episodes that occurred, mainly during the prolonged events in October. As stated in previous studies, ecosystem response has a non-linear relation with temperature, and simplistic interpretations of the effect of temperature increase on marine ecosystems should be avoided (Garrabou et al. 2009, Brander 2013, Brochier et al. 2013). Our observations at the Barcelona station suggest that the persistence of extreme seawater temperatures (>25.29°C at 5 m water depth or >22.88°C at 20 m water depth and <11.99°C at both depths) will make it possible to identify future extreme heat and cold wave events in the Barcelona coastal area. These thresholds correspond respectively to the 2^nd and 98^th percentile of the temperature recorded at 5 and 20 m water depth over the decade.

The T/S diagram from the CTD profiles collected off Barcelona shows a wide range of variability of temperature, salinity and density of the water masses during the study period, which is a common characteristic of coastal waters (Figs 12 and 15). Most measurements have properties of "old” Atlantic Water (oAW) or Continental Shelf Water (CSW) as defined in Salat et al. (2006), although some very dense waters (>1029 kg m^–3) found in the coastal region off Barcelona had properties characteristic of deeper water masses (Table 1). The highest density recorded in Barcelona coastal waters occurred in February-March 2005, January-March 2006 and March 2012, all periods corresponding to strong cascading or deep convection processes in the Gulf of Lions region (Salat et al. 2006, Palanques et al. 2012, Durrieu de Madron et al. 2013).

In the winter 2005 event, the dense shelf water cascading was observed at the head of the Cap de Creus Canyon in late December 2004. From late February to late March 2005, cascading occurred uninterruptedly and affected areas deeper than 750 m (Canals et al. 2006, Font et al. 2007, Puig et al. 2008). In the coastal zone of Barcelona, water densities greater than 1029 kg m^–3 were observed at least from early February to mid-March, with the highest density on 15 March 2005 (1029.25 kg m^–3). The transfer of dense waters from the Gulf of Lions towards the south along the Catalan continental shelf during the 2004-2005 event was reproduced by some oceanographic models (Ulses et al. 2008). These coastal dense waters can cascade downslope along their path and could be partially replenished by intrusions of slope waters over the shelf. In March 2005, Salat et al. (2006) identified water masses generated by shelf-cascading from a CTD section near the shelf break off Barcelona and suggested that such dense waters could favour the rise of LIW close to the surface, which is eventually brought over the continental shelf and therefore causes the near-disappearance of the typical shelf-slope front (Salat et al. 2006, 2009).

During the winter 2006 event in the NW Mediterranean, deep-reaching cascading pulses occurred in early January, late January and from early March to mid-April 2006 in the NW Mediterranean (Palanques et al. 2012). Marty and Chiavérini (2010) and Martin et al. (2010) described an intense convection and mixing process in the Ligurian Sea in February 2006 that caused an abrupt increase in temperature and salinity through the mixing of WMDW and LIW water masses. These authors suggested that this event was preconditioned and favoured by an increase in density in shallow waters (0-200 m water depth) and especially by the 2005 event that produced a decrease in the density gradient between surface and intermediate waters. Coastal waters in the Barcelona area also reached densities higher than 1029 kg m^–3 in late January and mid-March 2006.

Finally, the winter of 2012 was characterized by a significant cooling of surface water, especially on the inner and middle shelf of the Gulf of Lions, when density reached 1029.71 kg m^–3 on 13 February 2012 (Durrieu de Madron et al. 2013). From 5 February to mid-March 2012 several episodes of dense shelf water cascading occurred in the southern canyons of the Gulf of Lions, with the main cascading episode on 11 February 2012. The maximum density of Barcelona coastal waters that winter reached 1029.18 kg m^–3 on 22 February 2012, and values close to 1029 kg m^–3 were measured in the late January and mid-March surveys.

It is important to note that the main episodes of dense water formation and cascading in the western Mediterranean during the period 2002-2012 (events occurring in 2005, 2006 and 2012) can be clearly identified in the density records of the coastal waters of Barcelona, suggesting that advection of dense water from the Gulf of Lions and the Gulf of Roses (Ulses et al. 2008, Ribó et al. 2011) may reach or influence the Barcelona shelf. These events cause the weakening or disappearance of the shelf-slope front, which in turn favours exchanges between the coastal and oceanic waters (Salat et al. 2009). In fact, observations of some biological variables showed significant changes during those periods, probably related to the anomalous hydrographic situation caused by the extreme dense water formation events (Arin et al. 2013). For instance, a massive invasion of a jellyfish (identified as Pelagia noctiluca) was observed on several beaches along the Mediterranean Spanish coast (including the Catalan coast) during the summer of 2005. Pelagia noctiluca is an oceanic species that can reach the coast favoured by currents or winds (Graham et al. 2001). According to biological sampling data obtained at the study site, the phytoplankton species that typically produce the winter-spring blooms (mainly diatoms of the genera Chaetoceros and Pseudo-nitzschia) were partially replaced in 2006 by other species of diatoms (Bacteriastrum cf. delicatulum, Rhizosolenia cf. imbricata) and by a massive bloom of the nanoflagellate Phaeocystis sp. (Arin et al. 2013), usually found in open-sea oceanic waters. A similar phytoplankton composition was also observed in March 2006 at other sites of the central coast of Catalonia located north of Barcelona city (Sampedro et al. 2008), suggesting that the process had a wide regional range affecting the entire coast. The atypical hydrographic characteristics observed in the winters of 2005 and 2006 (with the weakening or disappearance of the shelf-slope front), in addition to favourable wind conditions, could have been the main causes of the expansion to the Catalan coastal waters of phytoplankton and jellyfish taxa of a more oceanic nature during these years (Arin et al. 2013).