On 8–9 September 2002, torrential rainfall and flooding hit the Gard region in southern France causing extensive damages and casualties. This is an exceptional example of a so-called Cévenol episode with 24 hour cumulative rainfall up to about 600 mm at some places and more than 200 mm over a large area (5500 km2). In this work we have used GPS data to determine integrated water vapor (IWV) as well as horizontal wet gradients and residuals. Using the IWV, we have monitored the evolution of the convective system associated with the rainfall from the water vapor accumulation stage through the stagnation of the convective cell and finally to the breakup of the system. Our interpretation of the GPS meteorological parameters is supported by synoptic maps, numerical weather analyses, and rain images from meteorological radars. We have evidenced from GPS data that this heavy precipitation is associated with ongoing accumulation of water vapor, even through the raining period, but that rain stopped as soon as the weather circulation pattern changed. The evolution of this event is typical in the context of the Cévenol meteorology. Furthermore, we have shown that the horizontal wet gradients help describe the heterogeneity of the water vapor field and holds information concerning the passage of the convective system. Finally, we have noticed that the residuals, which in theory should be proportional to water vapor heterogeneity, were also highly perturbed by the precipitation itself. In our conclusions we discuss the interest of a regional GPS network for monitoring and for future studies on water vapor tomography.
 In autumn, southern France along the Mediterranean arc is regularly the theater of extreme precipitation and flooding events producing societal damages including public and private goods destruction but also sometimes loss of lives. Such a strong event took place on 8–9 September 2002 in the Gard region. It can be categorized as a centennial catastrophe given the amount of precipitation and the extent of flooding. Indeed, the maximum value of daily accumulated precipitation recorded for 8 of September is 543 mm at Saint-Christol-lès-Alès in the Gard department, while the heavy precipitation occurred mainly in the afternoon of that day and the following night. Such a value is close to the actual mean accumulated precipitation over a year for that region. Furthermore, the geographical extent of the rainfall is extremely large as shown in Figure 1, where an area of about 5000 km2 received an accumulated amount of precipitation of more that 300 mm for a 48 hour period. Finally, the 8–9 September 2002 event accounts for a human loss of life of 13 plus 6 missing, while property damages add up to several tens of million Euros.
 This heavy precipitation event followed the classical development scheme associated with the so-called “Cévenol episodes” named after the Cévennes region which lies between the Massif Central mountainous region and the Mediterranean plains. In this scheme [Barret et al., 1994], a deep trough positioned between Ireland and Portugal generates a stationary cut of low positioned over Spain associated with cold stratospheric intrusion in altitude and a strong jet circulation which will produce lifting at its exit positioned over the Cévennes region. Meanwhile, a surface low develops over the Mediterranean Sea which induces a southern low level flux of warm and humid air in the lower layers of the atmosphere. Thus the encounter of the cold altitude air with the warm and humid surface flux plus the forcing due to the jet and the orography (the rise of the Massif Central and the funneling effect between those mountains and the pre-Alps to the east) produces a very unstable atmosphere prone to initiate deep convection and associated strong precipitation. Autumn is such a critical period because the artic cold air in altitude associated with the trough formation often reaches these latitudes for the first time after the summer and come across a warm Mediterranean sea and coastal regions. Hence more than 70% of rain events with more that 200 mm daily accumulated precipitation take place between 25 August and 15 November in that region [Barret et al., 1994].
 The societal impact of such events could be strongly mitigated if better forecasts of the expected amount of precipitation and its location were available. Usually, the main limitation for an accurate prediction of the precipitation and the modeling of the rain event dynamics is the poor knowledge of the water vapor field initial distribution and evolution [Emanuel et al., 1995; Ducrocq et al., 2002]. Indeed, although the amount of water vapor cannot be directly linked to precipitation amounts, water vapor can fuel the corresponding convective process.
 Nowadays, to measure water vapor in the atmosphere, meteorological services rely on standard synoptic radio soundings. However, even though such devices provide reasonably accurate measurements of water vapor profiles, they are far too sparsely distributed in space and time to support reliable forecasting of such rain events. Lately, Global Positioning Systems (GPS) has demonstrated its ability to monitor integrated water vapor (IWV) [Businger et al., 1996; Duan et al., 1996; Tregoning et al., 1998] with an accuracy comparable to other means of measurements (radio soundings, microwave radiometers, …) [Niell et al., 2001; Revercomb et al., 2003; Van Baelen et al., 2004], but also with good time resolution (better than hourly) and under all meteorological conditions. As more and more GPS are being deployed and operated in a continuous mode for geodetic purposes, they offer the potential for a dense and reliable water vapor measurement network. In this study, we have used the data collected by continuously or semicontinuously operating geodetic and geodynamical networks in southern France as well as some reference GPS stations in Europe.
 In the following sections, we will first introduce the GPS data used and their processing before focusing on the derivation of those parameters relevant to the meteorological documentation of the atmospheric water vapor content, distribution and variation. Then, we will present the meteorological context of this event. We will study the IWV distribution and evolution during the event while considering the associated rainfall. From the wet gradients and the residuals, we will describe the variability of the water vapor in the convective system. Furthermore, the effect of heavy rain on the GPS signals will be shown by a careful study of the residuals of the GPS processing. Finally, we will draw our conclusions and discuss the applications of GPS for weather monitoring and tomographic studies.
2. GPS Data and Processing
 The GPS data used in this study come from the continuously operating French networks RGP (Nationwide permanent GPS network from the Institut Géographique National: http://lareg.ensg.ign.fr/RGP/RGPhome.html) and REGAL (Alpine region GPS geodetic network: http://kreiz.unice.fr/regal), from the continuously operating GPS network of Catalonia CATNET (http://draco.icc.es/geofons/catnet/en/home.php), and from 3 GPS stations of the semicontinuously operating French network VENICE [Masson et al., 2003]. The GPS station MAHO in the Balearic Islands is maintained by the Royal Observatory of Spain. The geographical spread and density of those GPS stations is quite sparse but allows for the monitoring of the water vapor distribution and variations from the Balearic Islands in the Mediterranean Sea to the Alps and over the area of heavy precipitation and flooding.
 The GPS data processing was performed with the software GAMIT/GLOBK [King and Bock, 2000] in a quite conventional way. We compute in a first run the precise coordinates of the GPS stations in the ITRF 2000 frame [Altamimi et al., 2002] using 24 hour sessions, a cutoff angle of 10° and IGS final orbits. We use 10 GPS stations in Europe for the frame referencing. The final station coordinates are obtained by constraining the fiducial GPS stations to their ITRF2000 coordinates using the Kalman filter GLOBK [Herring et al., 1990] in a global solution. We find a repeatability of about 2 mm on horizontal and 5 mm on vertical baseline components. Then we perform a second run with loose constraints of 1 meter on the coordinates to evaluate hourly the tropospheric parameters [Bock et al., 2003], i.e., the zenith total delay (ZTD) and the total gradients. The lengths of the baselines are more than 1500 km to decorrelate the tropospheric parameters estimation from vertical positioning. The zenith delay a priori constraints, the variation of the Gauss-Markov process and the correlation time were set to 0.5 m, 0.01 m/√hour and 100 hours respectively and for the gradients 0.01 m, 0.01 m/√hour and 100 hours. Once again we use the IGS final orbits. We choose the “dry” and “wet” mapping functions described by Niell . We apply a sliding window session of 24 hours shifted by 12 hours to suppress the edge effect using the middle 12 hour of the session. The atmospheric parameters calculated during the GPS treatment are the ZTD, the north-south and the east-west total gradients at the elevation of 10°.
3. Wet Delay, Gradients, and One-Way Residuals
 The total atmospheric delay Latm between a GPS receiver and each visible satellite is a function of both the elevation angle ɛ and the azimuth angle α. Following Chen and Herring , it can be decomposed into a spherically symmetric contribution of the atmosphere Lsym, an azimuth-dependent contribution of the atmosphere due to its anisotropy Laz, and residuals S:
Lsym(ɛ) is only elevation-dependent. Lhz and Lwz are the zenith hydrostatic and wet delay, respectively, while mh(ɛ) and mw(ɛ) are the corresponding hydrostatic and wet mapping functions. In this study, we use the Niell mapping functions [Niell, 1996]. Laz(ɛ, α) is azimuth and elevation dependent. Lhns, Lhew, Lwns and Lwew are respectively the north-south and east-west components of the hydrostatic and wet gradients. maz is the gradient mapping function defined by Chen and Herring . Residuals S are then defined as the difference between the GAMIT final model results and the observations (using the ionosphere free linear combination LC). The ZTD obtained during the GPS treatment with the GAMIT software is the sum of Lhz and Lwz at the zenith or Lsym(90°). The north-south and the east-west gradients calculated by the GAMIT software are respectively Laz(10°, 0°) and Laz(10°, 90°).
 In order to study the water vapor contribution to the GPS signals, we have to extract the wet delays and gradients from the total atmospheric delay and gradients. To do so, we first derive the hydrostatic part of the zenith delay (Lhz) from surface pressure measurements (Figure 2a) interpolated at the station position following Davis et al. . The surface pressure measurements are the hourly synoptic observations of Météo-France (French National Weather Service). The accuracy of the pressure measurement is 0.1 hPa. The hydrostatic part of the total gradients (Figure 2b) is calculated from spatial variations of the ground pressure. From the pressure field near the GPS station, we calculate the spatial variations of the hydrostatic delay per unit of distance (km) in the north-south and east-west directions: Zhns and Zhew. Thus the equations for the hydrostatic gradients Lh and for the spatial variations of the hydrostatic delay Zh are:
where g is the horizontal gradient of the dry refractivity. Following Flores et al.  or Elòsegui et al. , we convert Zh to the hydrostatic gradients Lh assuming an exponential law in the hydrostatic refractivity such that:
where H, the scale height of the gradients in the hydrostatic delays is set to 13 km following Chen and Herring , who propose a larger-scale height for the gradients than those normally associated with the atmosphere, although they recognize that this assumption still needs to be confirmed by atmospheric simulation tests with a nonhydrostatic model.
 The effect of the hydrostatic gradient correction seems to be negligible in normal atmospheric conditions. On the contrary, during the passage of the convective system over the area during the studied event, the hydrostatic gradient amounts to about 20% of the total gradient which is not negligible (Figure 2b). Furthermore, the hydrostatic gradient is opposite to the total gradient, indicating that we need to take into account the hydrostatic gradient in order not to underestimate the wet gradient.
 Removing the hydrostatic contributions from the total delay leaves us with the zenith wet delay which can be converted into integrated water vapor (IWV) using the formula obtained for the Mediterranean area by Emardson and Derks  from more than 37000 radio-soundings and temperature surface measurements:
where Lw is the “wet” delay, I the integrated water vapor (IWV), TΔ the surface temperature minus the mean surface temperature of the area (289.76°K for the Mediterranean area) and a0, a1, a2 coefficients derived by Emardson and Derks  (respectively 6.324, −0.00177 and 0.000075). The accuracy of the equation (5) is estimated by the authors to be approximately 1%.
 The IWV represents the mean zenith integrated water vapor as seen by one GPS station and depends on the spatial distribution of the satellites. Typical amplitudes of the IWV are between 5 and 40 kg/m2 with an accuracy of about 1 kg/m2 compared to VLBI, radio sounding and radiometer [Niell et al., 2001]. The wet gradients represent the integrated linear heterogeneity of the water vapor above the GPS station in the direction of those satellites. The accuracy of the wet gradients is still poorly defined as the wet gradient is a parameter characteristic of GPS which is difficult to reproduce with other instruments like the radiometer [Gradinarsky et al., 2000]. The postfit residuals are the one-way (station-satellite) phase differences between the model obtained from GAMIT by least squares inversion and the observations. During “normal” atmospheric conditions, they are mainly due to multipath, uncorrected phase center variations and receiver clock error and thus they cannot be interpreted in terms of water vapor content. The magnitude of the residuals is about 1 mm of delay at the zenith. During particularly dynamic meteorological conditions, local atmospheric heterogeneities or hydrometeors can greatly enhance these residuals (as shown later in section 7.).
4. Meteorological Context of the 8–9 September 2002 Rain Event
 To study the meteorological background of this event, we will use 500 hPa geopotential analysis maps (Figure 3), surface wind and temperature analysis maps (Figure 4) and rain images (Figure 5) from the meteorological radar located near the town of Nîmes, France. The beam of the radar is 1.8°. Each image is calculated from 3 scans at 0.6°, 1.3° and 2.5° elevation above the horizon.
Figure 3 shows the 500 hPa geopotential analysis maps for Sunday 8 September and Monday 9 September 2002 at 1200 UTC. On the Sunday 8 September (Figure 3a), an upper cold pressure low is extended from Ireland to Spain by a deep trough. The low-level circulation associated to this low pressure on the Iberian Peninsula is a warm and moist south flow in the south France and in the Rhône Valley. This surface circulation is clearly seen on the Météo France operational model ARPEGE [Pailleux et al., 2000] analysis surface maps on Figure 4a. The convection starts on the Mediterranean Sea (0400 UTC) as seen on the rain radar images (Figure 5a) and in the land in the morning (Figure 5b). This deep convection organizes itself in a V-shape, typical for high precipitation event in French Gard area (Figure 5c). The edge of the V is positioned at the place of maximum convection where the clouds elevate the highest and where the precipitation is maximum. The clouds develop down-stream in a V shape fashion (Figure 5c) along the Massif Central contours and across the Rhône valley [Barret et al., 1994]. The orientation of the V-shape is given by the southwestern diffluent winds at the tropopause level (Figures 3a–3b). This deep convective system will give the main part of the precipitation. During the afternoon and the night of the 8 September, the region of precipitation moves slowly toward the east (Figure 5d).
 On Monday 9 September in the morning, the arrival of warm air from the Mediterranean Sea is still active (Figure 4b). Then, in the afternoon (Figure 3b), the axis of the trough changes from roughly north to south to northwest to southeast. The low-level flow begins to decay (Figure 4c) and the convection cells move toward the east (Figures 5e–5f). The change in the synoptic circulation corresponds to the end of the high precipitation in the south of France. More detailed description of the event and of the associated precipitation can be found in the work of Delrieu et al. . This event associated with deep stationary convection above the Gard region caused the historical precipitation described in the introduction and represented on Figure 1.
5. IWV Variations and Associated Rainfall
5.1. Description of the IWV Time Series
Figure 6 shows the temporal variation of the IWV from 7 to 9 September (days 250 to 252) 2002, at selected stations used in our analysis. The initial amount of water vapor is high around the Balearic Islands (30 kg/m2 in MAHO, day 250 1200 UT), increases going to the north (35 kg/m2 in CREU, day 250 1800 UT) and is maximum in MTPL (40 kg/m2, day 251 1200 UT) close to the rainfall. Hence during the south to north travel, the air is continuously loaded with water vapor from evaporation due to the Mediterranean Sea high surface temperatures at this period of the year (Figure 4; Delrieu et al. ). As the stations MAHO, CREU and MTPL are situated on the flux trajectory, one can notice that the water vapor maximum is shifted by about 6 hours between MAHO and CREU, while between CREU and MTPL the shift takes about one day indicating the stagnation of the mass of humid air which creates the favorable conditions for sustained convection.
 Four groups of stations can be distinguished. First, the southwestern stations (group 1: MALL, MAHO, EBRE, BELL and CREU), from the Balearic Islands to the eastern Pyrenees which document the inflow to the precipitation area; second, the stations on the western border of the core of the precipitation area (group 2: MTPL, AIGL); third, the stations to the east of the precipitation area, at the foothills of the pre-Alps mountains (group 3: CHRN, MARS, VERC, SJDS, MICH, GINA); and finally, the stations in the exit part of the convective system, further to the east and the north (group 4: SJDV, JOUX, FCLZ, GRAS, SOPH, AJAC).
 Considering the group 1 one can easily notice the increase of IWV during the day 250 of about 10–15 kg/m2. One notices as well its south to north progression in time and amplitude. Both are expected with the southern flow from the Mediterranean Sea (Figure 4). The IWV remain high during the end of the day 250 and the day 251. These stations within and around the Mediterranean Sea are located in the region of water vapor loading of the atmosphere: the area of convergence of water vapor of the south low-level flux (Figure 4). Around the western border of the rainfall zone, the group 2 shows an increasing IWV not only during the day 250 but also during the day 251. The increase from 20 to 40 kg/m2 of the IWV is spectacular for the MTPL station. This station location can be considered as the southern limit of the catastrophic rainfall event and demonstrates the high water vapor accumulation in that region prior to the start of the precipitation. Likewise, the AIGL station, which is in altitude on the first slopes of the Massif Central, exhibits relatively high values of IWV corresponding to the ascent of water vapor loaded convective clouds upon the orography (Figure 5c). The group 3 located on the eastern border of the zone of the catastrophic rainfall does not show a clear evolution of the IWV on day 250 up to the morning of day 251 and a very abrupt increase of the IWV at about 0600 UTC on day 251. This indicates that there is no water vapor loading in that region: IWV increases only when the convective system expands over those stations. One will notice that the observed step of 10 kg/m2 for the group 3 is generally preceded by a slight decrease of the IWV. Most of the precipitation has been observed between the groups 2 and 3 where, unfortunately, no GPS permanent station was operating during this period. The contrasted IWV behavior between these two last groups (2 and 3) fits the common description of Cévenol episodes with V shaped convective cloud formations. In our case, the group 2 are in the up-stream of the convective cell and monitor the buildup of water vapor and fuelling of the system. The group 3 shows a decrease of water vapor probably associated with low level convergence to the edge of the system at the time of convective initiation, and a later increase of water vapor corresponding to the development of the convective clouds above their region. Therefore, as demonstrated in Figure 2b, those stations of the group 3 will also experience a strong east to west wet gradient with higher values of IWV to the west, within the convective cloud build up zone during the day 251 above the Gard region. Finally, the stations of group 4 show signs of two parts of the event. Its Mediterranean sites exhibit, to a lesser proportion, some water vapor increase associated with the southern flux of warm and humid air (Figure 4). Its northern sites show signs of fairly perturbed but high levels of water vapor associated with the exit phase of the convective region during the night of 8 to 9 of September and the following day. For comparison, the water vapor variation at the GRAZ station in Austria is also shown to illustrate unperturbed meteorological conditions during those three days of the study. In a processing point of view, the similarity and simultaneity of the transition for all those stations located in a very small area is a good indication of the quality of the IWV estimates.
5.2. Spatial Evolution of the IWV
 To support the analysis above, we will now consider the evolution of the water vapor field revealed by successive IWV maps (Figure 7) over the area of interest. In order to plot the spatial variation of the IWV content corrected for the effect of altitude (the altitude of the GPS stations varies from sea level to more than 1500 m high in the Cévennes or in the Pyrenees), we plot the IWV relative to a reference distribution chosen at the beginning of the event: day 250 at 0300 UTC. The IWV maps obtained are determined by Hermit interpolation over the whole network. Hermit interpolation uses the value and their derivatives in each point of measure to constrain a polynomial interpolation. In this case, we use the east-west and north-south wet gradients as the horizontal derivatives of the IWV values. Thus using Hermit interpolation the IWV variations are well defined even in the areas without GPS stations but surrounded by several GPS stations. This is the case for the Gard department which corresponds to the region of maximum rainfall. Inversely, the borders of the map are noisier due to a lack of neighboring data.
 Although the GPS network is quite sparse, the large-scale spatial and temporal variations can be studied from the IWV spatial distribution maps. They clearly point out the water vapor displacement from the Mediterranean Sea (Figure 7a) to southern France and its accumulation over the Gard region. The high water vapor zone is limited to the west by the line CREU-MTPL, on the east by the line MARS-MICH and on the north by the station SJDV. This indicates that the area of high water vapor content is larger than the area of heavy precipitation as previously shown in Figure 1. The maximum IWV is located in the Gard region during about 24 hours between 0600 UTC day 251 and 0600 UTC day 252 (Figures 7b–7d) and is well correlated with the area and period of maximum precipitation. At 1200 UTC on day 252, the water vapor flux from the south becomes weaker and its orientation changes, the water vapor and the convective cell move toward the east (Figures 7e–7f) indicating the end of the stagnation and the dilution of the convective system. All these characteristics are well correlated with the rain images from Météo-France radars, especially the eastward motion of the rain system which marks the end of the catastrophic event (Figure 5).
5.3. Correlation Between IWV and Rain
 To investigate the correlation between IWV and rain at the ground level we will look at those GPS stations closest to the core of precipitation (AIGL, MTPL and CHRN) and which were almost collocated with rain gauges (less than 5 km). Rain gauges provide hourly accumulated precipitation data. The most intense rainfall has been recorded at the AIGL GPS station, with a maximum of 50 mm/hour at midnight on day 251. IWV and rainfall temporal variations do not show any clear correlation (Figure 8a). The increase of IWV is regular while the rain is abrupt. The maximum of IWV (30 kg/m2) occurs at the end of the rain time in early morning of day 252. It is interesting to point out that the increase of IWV continues during the rain. In MTPL (Figure 8b), the rainfall is less abrupt than in AIGL (25 mm/hour) but spreads over a longer period (about 12 hours). Once again there is a continual increase of water vapor during the rain and a maximum IWV at the end of the rain. This could indicate that the decrease of water vapor due to the precipitation is overcompensated by the south flux of water vapor which fuels the convective system and by evaporation. The measured rain at CHRN is quite different (Figure 8c). We see a high increase of IWV on the beginning of the day 251 followed by a small rain event (20 mm/hour) at noon. This is comparable to the phenomena observed at MTPL but with less intensity. However, a stronger rain event (30 mm/hour) is observed later at about 0600 UTC on day 252 and is directly correlated to a short term increase of water vapor. This is to be linked with intense but localized precipitation which can arise in the wake of the V-shape convective system that has developed over the Gard region and has far less impacts than the large and continuous rain experienced at the core of the system. To summarize, the large rain event occurred when the IWV reached high values of about 30 to 40 kg/m2 (water vapor fuels the convective system) but there is no direct relationship between IWV and the amount of precipitation.
6. Heterogeneity of Water Vapor Distribution: Study of Wet Gradients
 As the poor density of the GPS network available does not allow for detailed studies of the water vapor heterogeneities based on the IWV only, we will now study the meteorological information provided by the sum of the wet gradients and the residuals. It can be viewed as an accurate description of the horizontal heterogeneities of the atmosphere within the GPS station field of view.
 The sky plots in Figure 9 show the sum of the wet gradients and the residuals for the CHRN station during the day 252 for a period of 4 hours, while the black arrows represent the mean gradient and the ellipses its dispersion (RMS) during the corresponding periods. On these sky plots, one can easily observe the motion of the IWV associated with the convective precipitation event studied. From 0000 to 0800 UTC, the gradients reveal a high concentration of water vapor toward the west and the south. The sky plots show a clear east to west pattern, involving a relatively high gradient and a small RMS. This is consistent with the stagnation of the convective system over the Gard region (to the west) and its fuelling with water vapor coming from the Mediterranean (to the south). From 0800 to 1600 UTC, the gradients do not show any clear pattern and their RMS over four hours becomes larger than the signal. This can be related to the convective system extending above the station considered and filling the GPS field of view. After 1600 UTC, there is a clear (but small) west to east pattern in the sky plots. The corresponding west to east gradient associated with a small RMS is opposite to the gradient in the morning. This can be related to the fact that the convective system has broken up and is being advected further to the east. Observations from the other GPS stations in the vicinity of the heavy rainfall area are all consistent with the water vapor evolution scheme just described. Moreover, the water vapor evolution depicted here compares favorably with the meteorological radar observations of the rain system (Figure 5). Finally, one will also notice that the maximum amplitude of the wet gradients is not correlated with the rain itself. Actually, rain seems to occur when there are rapid changes in both the orientation and the amplitude of the wet gradients.
 In summary, the information provided by the wet gradients is a quasi-direct measure of the water vapor field horizontal variability within a horizontal scale of about 50 km. Thus a GPS station is capable not only to provide an observation of the integrated water vapor content of the troposphere above the receiver but can also provide a numerical measure of the azimuth variation of the water vapor distribution.
7. Investigation of the Residuals
 To get a more detailed look at the water vapor heterogeneity, we will now consider the residuals in an isolated way. Compared to the wet gradients, the residuals could provide the finest-scale heterogeneity (less than 50 km) of the water vapor field. They are not a mean model of the heterogeneity over all the satellites like the gradients but the remaining signal between one GPS station and one satellite. On the Figure 10, we have plotted the sky plots of the residuals along the GPS satellites tracks for the 8 September at MTPL (Julian day 251 of 2002). During the main rainfall from 0800 to 2000 UTC, the residuals are high and variable. Compared to average values of the residuals at this station, the residuals observed during the rainfall are two to three times larger. However, they do not allow identifying any water vapor organized structure. These high residuals do not result from multipath either as they are not elevation dependent. They could be due to an increase of electromagnetic (EM) effects of the fiberglass box of the GPS antenna during the rain. Indeed, the water on the fiberglass box could change its EM characteristics. However, if that was the case, the rain should only enhance preexisting patterns of the residuals (see http://www-gpsg.mit.edu/∼tah/web/japan_gps_met/GPSMetJapan.html) and that is not verified here. Another explanation could be a large and very high temporal variability of the water vapor during the rain with some interaction between evaporation and condensation. To test this hypothesis, we compute gradients and ZTD every 30 and 15 min to have a finer representation of the temporal variation of water vapor field. If the temporal variability of the troposphere was the main reason for those residuals, they should decrease using shorter meteorological GPS parameter intervals. We find only a limited decrease of the residuals but not strong enough to retrieve the typical amplitude of a normal day at these stations or of another GPS station (WTZR) in central Europe (Table 1). The unmodeled spatial variability of water vapor within the field of view of the GPS antenna could also contribute to the residuals. This kind of hypothesis could be tested with a local tomography of water vapor [Champollion et al., 2004]. The tomography can however not be achieved for this study because of the too large spacing between GPS stations. Finally, the most significant part of the residuals could be due to liquid water in the troposphere in the form of rain, ice and clouds. The enhancement of the residuals is well correlated in time with the precipitation with a maximum for MTPL and CHRN at about 1200 UTC the 8 September. The levels of residuals found in our study are in good agreement with the absorption model described by Solheim et al.  who find 5 mm/km of surface delay for rainfall of 50 mm/hour with a scale height of 3 or 4 km. Further studies with high resolution numerical weather simulations confirm this hypothesis (H. Brenot et al., manuscript in preparation, 2004).
Table 1. Mean RMS of the Residuals Between 0000 and 2400 UTC, Julian Day 251 for the GPS Stations MTPL, CHRN, and WTZRa
ZTD and Gradients Evaluated Every 2 Hours
ZTD and Gradients Evaluated Every Hour
ZTD and Gradients Evaluated Every 30 min
ZTD and Gradients Evaluated Every 15 min
The ZTD and gradients are evaluated every 2 hours, 1 hour, 30 min, and 15 min. The italic numbers indicate respectively the RMS of the residuals between 0000 and 0600, 0600 and 1200, 1200 and 1800, and 1800 and 2400 UTC. The mean RMS is for the whole 24 hours.
8.39.616.113.5 mean 11.9 mm
8.09.015.813.2 mean 11.5 mm
7.68.315.512.3 mean:10.9 mm
6.47.315.311.9 mean 10.2 mm
220.127.116.115.7 mean 14.7 mm
7.1 13.1 22.6 15.6 mean 14.6 mm
6.818.104.22.168 mean: 13.5 mm
6.011.120.112.4 mean 12.4 mm
22.214.171.124.9 mean 6.8 mm
126.96.36.199.5 mean 6.4 mm
188.8.131.52 6.5 mean 6.4 mm
184.108.40.206.0 mean 6.2 mm
 IWV temporal variations (Figure 5), IWV spatial variations (Figure 6) and wet gradients temporal variations (Figure 9) can improve the understanding of large rainfall events. They allow an accurate and continuous description of the water vapor field variations before, during and after the heavy precipitation.
 In our case study, the IWV reveals that the water vapor flux is initiated in the Mediterranean Sea south of the Balearic Islands and moves northward parallel to the Spanish shoreline. The water vapor content increases during the northward motion. The velocity of the flux decreases while reaching the French shoreline. Finally, the maximum water vapor content is observed in MTPL, just south of the maximum rainfall zone. Different temporal variations of IWV are observed between the GPS stations west and east of the rainfall area. The water vapor increases continuously and linearly for the stations southwest of the raining area. They are located in the “loading” zone. East of the raining area, the IWV variations are more complex, with successive increases and decreases, indicating the complexity of the phenomena close to the rainfall zone at time of precipitation but especially once the convective system breaks up. These interpretations are confirmed by the ARPEGE analyses and the rain images from radars (Figures 4 and 5).
 This study also illustrates an important result about the wet gradients: a single GPS station can provide partial information on the heterogeneity of the troposphere by extracting the wet gradients. During the passage of the rain system, the wet gradients are weak and highly variable. Before and after the rain, the wet gradients give clear information of the lateral heterogeneity of the atmosphere. They indicate the contrast of humidity between the different parts of the meteorological system. For the monitoring of air mass heterogeneity, the wet gradients are a good indicator which could be available in near real time like other meteorological parameters. They could be used for estimating the time of arrival of a front above a GPS station and, thus, for checking and updating the event chronology in numerical weather prediction forecasts.
 Theoretically, the study of the residuals provides the finest information about the water vapor heterogeneity which cannot be modeled by the IWV and the gradients. The residuals also include the noise due to the liquid water, the multipath, the errors of the mapping function, etc. The MTPL data indicate that the residuals increase significantly during the large rainfall probably due to rain scattering. If this observation is confirmed, GPS residuals could be investigated in relation with the characterization of the rain. Furthermore, the modeling of the residuals due to the rain could be useful to correct the gradients for meteorological applications like GPS water vapor tomography [Champollion et al., 2004]) or data assimilation in numerical models [Gutman et al., 2004].
 This study has been conducted using the current permanent GPS network of southern France and Spain. Further studies need a denser GPS network recording data during a long period to get a database covering several catastrophic rainfall events. A large database will allow to characterize the catastrophic rainfall situations and to distinguish these events from standard autumnal precipitation. A field experiment could be conducted next autumn with more temporary GPS stations from Marseille to Agde, i.e., covering the zone of the maximum rainfall with a typical spacing of 50 km. From these data, we will be able to resolve the small-scale variations in 3-D of the water vapor with the tomographic software we have developed [Champollion et al., 2004] and get an insight into monitoring and the dynamics of strong rain events. GPS stations have been located close to the shoreline to study the potential of GPS to explore the troposphere above the Mediterranean Sea, to provide a precursor of the catastrophic rainfall events. In ongoing work, gradients and residuals will be carefully studied.
 This work was partially supported by the Institut des Sciences de la Terre, de l'Environnement et de l'Espace de Montpellier (ISTEEM) and by the Observatoire Hydrométéorologique Méditerranéen Cévennes-Vivarais (OHMCV). We thank Philippe Collard, Laboratoire Dynamique de la Lithosphère (LDL), for his work in the installation and the maintenance of the VENICE semipermanent GPS network, Sandrine Anquetin and Simon Yates, Laboratoire d'étude des Transferts en Hydrologie et Environnement (LTHE), for providing the rain gauge data. We would like to thank the three anonymous reviewers for their detailed and relevant comments of this paper.