Air Masses Origin and Isotopic Tracers: A Study Case of the Oceanic and Mediterranean Rainfall Southwest of France

Abstract

Aquifers recharge mainly by local rainfall, which depend on the air mass humidity and orographic lifting, causing rain. The stable isotopes of the water molecule, i.e., oxygen-18 and deuterium, are useful tracers to determine the water source origin. Moreover, the calculation of the deuterium excess enables one to differentiate between the air masses from the Atlantic Ocean or the Mediterranean Sea. A transect from one coast to the other one and going through the city of Toulouse have been made to sample the groundwater and determine their isotopic characteristic. A monthly rainfall sampling has also been done over one year, close to the city Toulouse, to see how the d-excess values range over the season. The discussion replaces these results in available isotopic data.

1. Introduction

France presents a wide range of coasts and is influenced by both the Atlantic Ocean and the Mediterranean Sea. The morphology of this country, which impacts the rainfall pattern, is complex, with the Massif Central in the center, the Alps to the east and the Pyrenees to the south. The main processes controlling the δ¹⁸O and δD isotopic signatures in precipitations were summarized by Rozanski et al. [1]; i.e., the rainfall amount, continental and altitude effects and the origin of air masses. For France, some pioneer works have studied the isotopic pattern of rainfall, such as Celle et al., Celle-Jeanton et al., Ladouche et al. and Millot et al. [2,3,4,5], but still, some areas lack for valuable data, like the Southwest area. It is, therefore, important to constrain the signature of the atmospheric signal in these geographical and geomorphological contexts by means of a rainfall-monitoring network and groundwater measurements.

The Southwest of France presents the characteristics of having two major winds blowing in an opposite direction. For instance, in Toulouse, the northwest wind (280° to 340°), called “Cers”, blows during 43% of the year, bringing the moisture from the Atlantic Ocean, and the southeast wind (120° to 180°), called “Autan”, blows during 29% of the year, bringing the Mediterranean influences. Therefore the airport runways are oriented N-W/S-E, the planes taking them from one end or the other depending on the wind origin.

The Autan wind is a föhn-type wind deriving from the Marin wind from the Mediterranean and blowing over the Languedoc into the Tarn and the Garonne valleys, affecting the Lauragais (the hilly area between Castelnaudary and Toulouse) and the Toulouse area. Channeled and intensified by the narrowing lowlands between the Pyrenees and the south of the Massif Central, it undergoes sudden acceleration between the Corbières and the Montagne Noire (Venturi effect). Gusts can exceed twice the mean speed, possibly enhanced by lee-wave activity.

To understand the Atlantic Ocean and the Mediterranean Sea on the southwest rainfall of France, the present work summarizes over 75 isotopic measurements of shallow groundwater, used as rainfall natural gauges, located between these two coasts. This study is completed by an 18 months’ rainfall survey near Toulouse in view to follow the air masses origin for the rainfall over the season and the influence of the Mediterranean income mainly through the Autan wind.

2. Experimental Section

2.1. Study Area

The Southwest of France stretches between the Atlantic and the Mediterranean coast over 350 km; see Figure 1, Figure 5. For the groundwater, the sampling places were taken in alluvial plains, i.e., along the Garonne and Adour valley at the west and along the Aude valley at the east. The connection between the two basins is Seuil de Naurouze (189 m) located 40 km southeast of Toulouse. Farm wells or piezometers, if available, were used for the shallow groundwater sampling. Typical water depth ranges between 2 and 12 m. The longer groundwater survey has been made near Verdun sur Garonne, 35 km downstream (northwest) of Toulouse, in a farm well (depth 2–4 m), one km away from the Garonne River. It is located in the middle of the Garonne Channel and would be classified as mixed bedrock-alluvial stream [6], and the valley contains a classic flight of clay terraces that represent an episodic bedrock valley deepening and punctuated by lateral migration of the deposition of coarse gravels and sands.

Along the west to east transect, the rainfall cumulates at the feet of the Western Pyrenees, with 1156 mm per year in Dax and a little less for Cestas-Pierroton, located north of Bordeaux with 920 mm. After, the rainfall amounts lower along the Garonne Valley with 763 mm in Agen and 660 mm in Toulouse. It increases slowly in the area of Carcasonne 736 mm, due to the proximity of the mountains, before slowing down again in the direction of the Mediterranean Sea: 609 mm in Narbonne, 549 mm in Perpignan and 605 mm in Sète. On the contrary, the evaporation enhance from west to east due to the increasing insulation.

Figure 1. The Southwest of France with the localization of the sample sites with the typical δ¹⁸O value of the groundwater (in white) and the upstream basin (in red). The resulting isovalue contour for δ¹⁸O = −5‰, −6‰ and −7‰ are given with a white line, and the two dominant wind directions are given by both arrows.

Figure 1. The Southwest of France with the localization of the sample sites with the typical δ¹⁸O value of the groundwater (in white) and the upstream basin (in red). The resulting isovalue contour for δ¹⁸O = −5‰, −6‰ and −7‰ are given with a white line, and the two dominant wind directions are given by both arrows.

2.2. Rainfall Sampling

Close to our isotopic laboratory in Auzeville, 8 km southeast of Toulouse, a rainfall sampling was installed during June 2011. Its consist of a polypropylene funnel (22 cm diameter) covering a 5 L polypropylene jerrycan, containing 300 mL of paraffin oil to avoid any evaporation process. The rainfall aliquots were sampled monthly, between July 2011 and December 2012. The meteorological data used were obtained from the close INRA station (less than 1 km) and compared with the long-term Toulouse airport station, Blagnac, where the record started in 1809, and located northwest, at 18 km. For each monthly sample, 10 mL were used for δ¹⁸O and δD determination.

2.3. Groundwater Sampling

The shallow groundwater survey started in 1997 at Monbequi near Verdun sur Garonne in farm wells and piezometers to follow the influence of the Garonne River in this meander area [7,8]. The upper well was chosen as the local ground water reference and samplings were made over 6 years. To get a wider understanding of the alluvial groundwater characteristic, complementary samplings were done along the Garonne Valley between 2004 and 2007, for the Adour Valley between 2005 and 2006 and at the Seuil de Naurouze and Aude Valley in 2010.

2.4. Isotopic Measurements

Glass vial of 10 mL with tight caps were used for water sampling. The vials were kept at stable temperature before the measurement of the δ¹⁸O and δD determination on a continuous flow isotope ratio mass spectrometer. Before 2007, the water samples were send to an iso-analytical laboratory in England (ANCA-GSL and GEO 20–20 IRMS, Europa Scientific, Crewe UK). Each water sample was measured in triplicate for each isotope ratio. The overall mean standard deviation (SD) for the δ¹⁸O values was around ±0.15‰, and the mean SD for the δ²H values was ±1.7‰. From 2010, the measurements were done on our own isotopic platform, Shiva (Isoprim 100 and Geo-multi-flow, Elementar, Hamburg, Germany). Each water sample was measured in duplicate. The mean standard deviation (SD) for the rainfall measurements was around ±0.29‰ for δ¹⁸O, and the overall mean SD was ±2.5‰ for δ²H.

The results are given relative to V-SMOW standards from IAEA. The deuterium excess was calculated using the Global Meteorological Water Line (GMWL), as defined by Craig [9] and completed by Dansgaard [10]:

d-excess = δD – 8 × δ¹⁸O

(1)

A value of d-excess around 10 or below, i.e., similar to the GMWL, was taken as originating from Atlantic moisture and a value around 14 [2] as moisture with water recycling as one coming from the close West Mediterranean basin.

3. Results and Discussion

3.1. Rainfall Results

The data were obtained between July 2011 and December 2012. The annual amount of rainfall for 2011 was 538 mm, and for 2012 it was 548 mm in the INRA station and around 20% over the amount values from Blagnac Airport station. These numbers are under the 30 years mean (CLINO period 1961–1990 [11]), 671 ± 121 mm per year monthly, as since 2003, the Toulouse area is in a dry period. The obtained isotopic value for δ¹⁸O ranges from −10.7‰ to −4.0‰, showing the continental influence, with a mean monthly temperature ranging from −2.5 °C (February 2012) for the minimum to +30.4 °C (August 2012) for the maximum. Table 1 reports the obtained isotopes values for the monthly rainfall, with the meteorological data from the nearby INRA station.

In Figure 2, both years are plotted along a whole year and present a similar pattern. The δ¹⁸O signal presents the more depleted values in winter and the less depleted in summer, following the temperature shift. The negative peak from February 2012 corresponds to a cold period, until −12.5 °C on February 9, with one week of snow. The d-excess displays more erratic variations, perhaps with some evaporative process in summer (July) and a possible Mediterranean influence in October.

Figure 3 gives the representation of δ¹⁸O versus δ²H for both years. For 2011, the regression gives in 2011 a slope of 7.70 and a d-excess of 11.28 with R² = 0.979, and in 2012, the slope is equal to 7.70 and a d-excess of 9.85 with a R² = 0.909. Both sets are very close with the Global Meteorological Water Line (GMWL) defined by Craig 1961 [9]. The point above the GMWL (δ¹⁸O = −7.83‰, d-excess = +22.12) corresponds to a possible Autan wind influence with the incoming of Mediterranean rain. The weighted mean (w-mean) of δ¹⁸O or the d-excess can be calculated by summing the monthly amount of rainfall (rainfall amount_month) relative to the total rainfall for one year and multiplying both monthly isotopic values, according to the following equation:

δ¹⁸O_w-mean = Σ ^{i = 1 to 12} δ¹⁸O_month × Rainfall amount_month ÷ Rainfall amount_year

(2)

The obtained value for the 2012 values is δ¹⁸O_w-mean = −6.32‰ ± 0.25‰ and a d-excess_w-mean = 11.76 ± 0.59.

Table 1. Isotopic results, calculated d-excess and meteorological conditions for the rainfall samples near Toulouse.

Month	δ18O	δ2H	d-excess	Rainfall	Min. T	Max. T
	(‰)	(‰)		(mm)	(°C)	(°C)
July 2011	−4.48	−28.15	7.69	86.5	14.9	25.7
August 2011	−4.00	−19.02	12.98	21.5	16.3	29.0
September 2011	−5.18	−27.18	14.24	73.5	14.8	27.2
October 2011	−6.59	−36.73	15.98	24.5	9.6	21.7
November 2011	−10.71	−72.56	13.12	31.0	9.6	15.9
December 2011	−5.62	−30.45	14.51	53.0	5.0	12.1
January 2012	−6.55	−40.87	11.53	39.0	3.8	10.3
February 2012	−10.22	−71.81	9.95	4.0	−2.5	6.0
March 2012	−5.80	−32.00	14.40	22.0	4.1	17.5
April 2012	−6.71	−44.17	9.51	69.0	7.6	16.2
May 2012	−4.80	−24.84	13.56	75.5	11.6	22.2
June 2012	−4.67	−27.23	10.10	53.5	15.0	26.5
July 2012	−4.53	−29.61	6.63	58.0	14.7	27.5
August 2012	−6.28	−39.35	10.89	48.5	17.5	30.4
September 2012	−5.25	−28.96	13.05	26.0	13.9	24.7
October 2012	−7.83	−40.53	22.12	53.0	11	20.5
November 2012	−8.89	−55.92	15.20	49.5	6.8	14
December 2012	−8.09	−59.80	4.93	50.5	4.6	11.6

Table 1. Isotopic results, calculated d-excess and meteorological conditions for the rainfall samples near Toulouse.

Month	δ18O	δ2H	d-excess	Rainfall	Min. T	Max. T
	(‰)	(‰)		(mm)	(°C)	(°C)
July 2011	−4.48	−28.15	7.69	86.5	14.9	25.7
August 2011	−4.00	−19.02	12.98	21.5	16.3	29.0
September 2011	−5.18	−27.18	14.24	73.5	14.8	27.2
October 2011	−6.59	−36.73	15.98	24.5	9.6	21.7
November 2011	−10.71	−72.56	13.12	31.0	9.6	15.9
December 2011	−5.62	−30.45	14.51	53.0	5.0	12.1
January 2012	−6.55	−40.87	11.53	39.0	3.8	10.3
February 2012	−10.22	−71.81	9.95	4.0	−2.5	6.0
March 2012	−5.80	−32.00	14.40	22.0	4.1	17.5
April 2012	−6.71	−44.17	9.51	69.0	7.6	16.2
May 2012	−4.80	−24.84	13.56	75.5	11.6	22.2
June 2012	−4.67	−27.23	10.10	53.5	15.0	26.5
July 2012	−4.53	−29.61	6.63	58.0	14.7	27.5
August 2012	−6.28	−39.35	10.89	48.5	17.5	30.4
September 2012	−5.25	−28.96	13.05	26.0	13.9	24.7
October 2012	−7.83	−40.53	22.12	53.0	11	20.5
November 2012	−8.89	−55.92	15.20	49.5	6.8	14
December 2012	−8.09	−59.80	4.93	50.5	4.6	11.6

Figure 2. Monthly variation of (a) δ¹⁸O and (b) d-excess with error bars for the rainfall in 2011 (dotted line, no symbol) and 2012 (plain line, cross symbol) near Toulouse.

Figure 2. Monthly variation of (a) δ¹⁸O and (b) d-excess with error bars for the rainfall in 2011 (dotted line, no symbol) and 2012 (plain line, cross symbol) near Toulouse.

Figure 3. Relationship between the δ¹⁸O and δ²H rainfall values for 2011 and 2012 compared to the GMWL line (dotted line).

Figure 3. Relationship between the δ¹⁸O and δ²H rainfall values for 2011 and 2012 compared to the GMWL line (dotted line).

3.2. Groundwater Results

3.2.1. Reference Well

The survey of the reference well for the groundwater over six years (see Figure 4) reveals that the δ¹⁸O values range from −6.18‰ to −7.10‰.The overall mean value of δ¹⁸O= −6.60‰ ± 0.24‰ (n = 31), whereas the annual mean values range from −6.43‰ to −6.86‰. The seasonal pattern appears very reduced (Δδ¹⁸O = 0.2 units) for these 31 samples, with a slight depletion in spring. This dampened isotopic amplitude (A_GW) response compared to the rainfall isotopic amplitude (A_rainfall) can be used to calculate the mean residence time (t_mr) according to the exponential model equation of Stichler and Herrmann [12]:

t_mr= 0.5π × (A_rainfall²/A_GW² − 1)^0.5

(3)

This calculation gives a residence time of about five years.

Figure 4. Variation of the δ¹⁸O values of the reference groundwater well near Verdun sur Garonne (between 1997 and 2003) over the season. The solid line represents the polynomial regression line.

Figure 4. Variation of the δ¹⁸O values of the reference groundwater well near Verdun sur Garonne (between 1997 and 2003) over the season. The solid line represents the polynomial regression line.

3.2.2. Groundwater between Atlantic and Mediterranean Coasts

The numerous alluvial ground water sample along the Garonne, Adour and Aude Valleys shows that there is a gradient from around δ¹⁸O = −5.0‰ close to the Atlantic coast (−4.6‰ in Dax and −5.4‰ in Bordeaux) and slowly becoming more depleted when coming more inland. At Verdun/Garonne, 50 km downstream of Toulouse, and until Seuil de Naurouze, the highest point (189 m) where the water flux divides itself between the Atlantic and the Mediterranean slope, the δ¹⁸O reaches −6.6‰. The continental effect continues on the east slope until Raissac, 25 km before the Mediterranean Sea, with a value of δ¹⁸O around −6.8‰. Along this sea coast, the isotopic values become less depleted, with δ¹⁸O value close to −5.5‰.

On the contrary, the d-excess starts close to 10 (i.e., the value of GMWL) along the Atlantic coast, before dropping inland, until Toulouse, around 6. From Seuil de Naurouze, the d-excess increases from 8.2, to 9.8 in Raissac, before reaching 12.6 at La Franqui. The Mediterranean Sea is a closed system and displays a higher d-excess value, around 14 [2]. The effect of the Mediterranean Sea through the Autan wind affects the d-excess, meaning that the water vapor recycles until Seuil de Naurouze, but the isotopic signal of the of the Continental effect coming from the Atlantic coast stops only a few ten km before reaching the Mediterranean coast, see Figure 5.

Figure 5. Continental gradient from the west Atlantic coast to east Mediterranean coast: mean isotopic values (δ¹⁸O, d-excess) for the different alluvial ground water stations along the Garonne, Adour and Aude Valleys. The altitude of the station is given between brackets.

Figure 5. Continental gradient from the west Atlantic coast to east Mediterranean coast: mean isotopic values (δ¹⁸O, d-excess) for the different alluvial ground water stations along the Garonne, Adour and Aude Valleys. The altitude of the station is given between brackets.

3.3. Discussion

Most shallow groundwater is of meteoric, i.e., atmospheric origin. Rainwater directly infiltrates the ground or indirectly via the inflow of surface water or from bank storage in streams [13]. Shallow and locally-derived ground waters are often used to characterize the isotopic content of meteoric waters, due to the conservative nature of the stable isotope composition of water in an aquifer [14].

Unconsolidated sediments, like in a river valley, are excellent and most efficient aquifers. Their porosity and permeability are usually high [13]. We have measured the groundwater velocity in Verdun near our reference well, and the velocity ranges from 2.1 to 3.2 m/day [15]. Such alluvial plains present high precipitation response to rainfall, and the residence time of ground water is short. In general, alluvial shallow groundwaters are known to be two to 50 years old [16]. In our case, with the equation of Stichler [12], we found a resident time of five years for our groundwater reference well.

On the contrary, deeper groundwater in the Adour-Garonne basin is characterized by more depleted values than the actual mean isotopic rainfall, with values ranging from δ¹⁸O = −5.6‰ to −10.6‰ [17]. For instance, in the Southwest of France, we found isotopic values ranging from δ¹⁸O= −7.2‰ to −7.8‰, (Lambs, unpublished results) for many tens of meters-depth bore wells. Such heterogeneity in the δ¹⁸O signature for a Paleocene aquifer reflects a variable recharge, either in space and time. The most depleted values correspond to a water recharged with a colder climate than the present one [17].

From the isotopic results around Toulouse, there is very good agreement between the Verdun groundwater annual average value (δ¹⁸O_mean = −6.60‰ ± 0.25‰) and the rainfall (δ¹⁸O_mean = −6.63‰ ± 1.81‰). For the calculated d-excess, there is a small shift with a mean value of d-excess_mean = 6.0 ± 1.7 for the groundwater and d-excess_mean = 11.8 ± 4.43 for the rainfall. Notice also that the groundwater taken at the Naurouze pass in 2010 gives similar values (δ¹⁸O = −6.80‰ ± 0.28‰, d-excess = 8.2 ± 1.9) compared to Verdun groundwater sampled between 1997 and 2003.

On a wider scale, the isotopic fractionation with the altitude is around −0.28 δ¹⁸O per mil for 100 m of elevation [2]. Along our transect, as the mean values of the groundwater around Bordeaux are δ¹⁸O = −5.6‰, at the highest point, Seuil de Naurouze (189 m), the altitude isotopic should at least be −6.2‰, but as the mean Lauragais hill is around 290 m, a correct value would be −6.5‰. Another way is to calculate the continental effect with the ratio of −3.2 δ¹⁸O per mil for 1000 km inland [5]. From the Atlantic coast at the level of Bordeaux until Seuil de Naurouze, there is 330 km, which should give a fractionation of −1.06, i.e., around −6.66‰, which is in better accordance with the measured values. If one calculates the continental fractionation until Raissac, 420 km from the Atlantic coast, the new δ¹⁸O would become −6.94‰, a value more depleted than the observed mean value of −6.83‰.

Rainfall coming from the western Mediterranean basin is known to present less depleted δ¹⁸O values, but with a higher d-excess value, around +14 [3,18]. Such an influence is seen on groundwater δ¹⁸O values of la Franqui and perhaps also in the higher d-excess of the Raissac area. Even in Toulouse, in October 2012, the abnormal d-excess of the rainfall could come from this Mediterranean inflow. In general, the Mediterranean rainfall seems to be located much closer to the coast, a few tens of kilometers wide. Only the black Autan wind, a particular case of the Autan wind blowing northwest, can bring Mediterranean moisture more inland. However, the amount of this East Mediterranean rainfall remains low compared to the West Atlantic rainfall. The Autan wind is a continental high pressure wind bringing heat and dryness and is influenced by the local orography. Even if different meteorological models try to understand this particular wind [19,20,21], it is often not announced in the weather forecast.

Table 2 reports the rainfall isotopic data available in the Global Network of Isotopes in Precipitation (GNIP) database from IAEA [22]. For Toulouse, the data is from the present work (year 2012), as there is no other data on the GNIP database. However, it is possible to get the calculated interpolated data from the area of Toulouse [23], which is δ¹⁸O = −6.2‰ ± 0.3‰. This value is a little less than our mean value (δ¹⁸O_mean = −6.6‰ ± 1.8‰), but equal to our weighted mean: δ¹⁸O_w-mean = −6.32‰ ± 0.25‰. For the slope between the δ¹⁸O and δD values, only Toulouse presents a value close to the GMWL (respectively, 7.70 and 8.00). All the other places on both coasts display a lower slope, due to a smaller δ¹⁸O. It is not necessarily a problem of coastal influence or the evaporation process. In fact, the GMWL as a global line is made of many small local lines with slopes that are often smaller than eight. There is a good correspondence between the calculated δ¹⁸O weighted mean of Bordeaux (in fact, Cestas-Pierroton) and our mean groundwater of this area (respectively, −5.69‰ and −5.59‰) and also the calculated δ¹⁸O weighted mean of Dax and our mean groundwater of this area (respectively, −4.59‰ and −4.86‰). With these δ¹⁸O weighted means, the continental effect from west to east between Bordeaux and Toulouse is around one unit and the latitude effect between Bordeaux and Dax, also one unit of δ¹⁸O. One can also notice the equivalent of δ¹⁸O weight mean values of Dax and Montpellier (respectively, −4.59‰ and −4.17‰), nearly on the same latitude, but on a different sea coast. The calculated weighted d-excess mean is always high, i.e., between nine and 12, and only in Avignon, it drops at around eight.

The study of the West Mediterranean influence is complex, as it is a transition zone between the cool North Atlantic air masses and the warm and wet air flowing from the Mediterranean basin. The isotopic signal of the air masses from these different origins crossing the Mediterranean may be modified by water vapor produced in the Mediterranean [3]. The d-excess value of the water vapor of the Mediterranean region results from the intensive evaporation near the coast, under conditions of a large humidity deficit [24]. All these particular features from the Mediterranean water vapor reveal the importance of the study to understand the local climate by monitoring numerous and long-term rainfall and groundwater sampling.

Table 2. Comparison of the isotopic features of the GNIP stations and our Toulouse station.

City	Slope	d-excess	R2	δ18Ow mean	d-excessw	δ18O range	Rainfall	Year
				(‰)		(‰)	(mm)
Dax	6.09	0.32	0.948	−4.59 ± 0.95	9.71 ± 1.24	−6.84–−2.25	1156	1999–2005
Bordeaux	6.90	3.90	0.925	−5.69 ± 0.65	10.18 ± 0.32	−7.16–−4.33	920	2007–2009
Toulouse	7.70	9.86	0.909	−6.32 ± 0.25	11.76 ± 0.59	−10.71–−4.00	548	2012
Montpellier	6.49	3.07	0.825	−4.17 ± 0.14	9.07 ± 2.07	−6.65–−1.79	595	1997–1998
Avignon	7.19	2.31	0.984	−5.49 ± 1.20	7.39 ± 2.95	−7.83–−2.23	619	1997–2009

Table 2. Comparison of the isotopic features of the GNIP stations and our Toulouse station.

City	Slope	d-excess	R2	δ18Ow mean	d-excessw	δ18O range	Rainfall	Year
				(‰)		(‰)	(mm)
Dax	6.09	0.32	0.948	−4.59 ± 0.95	9.71 ± 1.24	−6.84–−2.25	1156	1999–2005
Bordeaux	6.90	3.90	0.925	−5.69 ± 0.65	10.18 ± 0.32	−7.16–−4.33	920	2007–2009
Toulouse	7.70	9.86	0.909	−6.32 ± 0.25	11.76 ± 0.59	−10.71–−4.00	548	2012
Montpellier	6.49	3.07	0.825	−4.17 ± 0.14	9.07 ± 2.07	−6.65–−1.79	595	1997–1998
Avignon	7.19	2.31	0.984	−5.49 ± 1.20	7.39 ± 2.95	−7.83–−2.23	619	1997–2009

4. Conclusions

The present study is the first one to provided isotopic rainfall data for the Toulouse area in connection with numerous alluvial groundwater sampling over the Southwest of France. These results reveal that this area is influenced by both the Atlantic and the Mediterranean climate, but also, a continental effect is perceptible through the wide isotopic range. The Mediterranean influence is mainly brought by the Autan wind, but the isotopic composition of the groundwater is only influenced closer to a few tens of kilometers from the Mediterranean shore. Only some d-excess higher value can reveal it. More sampling of rainfall at the month scale still needs to be done for this area to better understand this specific climate. Furthermore, sampling of individual special rain events, like after the Autan wind, is now also performed for trying to refine these possible Mediterranean moisture inflows.