Istituto di Scienze dell'Atmosfera e del Clima Institute of Atmospheric Sciences and Climate 
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Latest Month  Latest Season  Latest Year  Yeartodate  LongTerm Analysis  Info 
Latest Month AnalysisAUGUST 2017

Latest Season Analysis(Winter:DJF; Spring:MAM; Summer:JJA; Autumn:SON) SUMMER 2017
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LongTerm Analysis(deviation from the 19712000 mean) METEOROLOGICAL YEAR (December to November)
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THE DATA SETAt present day, many of the historical Italian Meteorological Observatories are closed and for those still working it is difficult to obtain data in an automatic and near real time way. For this reason, the historical Observatories records, when possible, were merged with the modern Air Force network to get a series wich is updatable in near real time and automatically via GSOD Network managed by NCDC/NOAA. The whole data set (both merged and not merged series) has been homogenized with statistical techniques to eliminate all the nonclimatic signals due to station history (changes in the instruments, instruments/station relocation, changes in the observations riles, and so on). See Brunetti et al. (2006) for details about data homogenization and Venema et al. (2012) for details about the performances of the mostly used homogenization techniques. The homogenization is a necessary step to provide time series with a longterm signal as close as possible to the real climate signal. The figures show the data set with different symbols for stations wich are updated in near real time and stations not updated. 

An example: if we average the temperature records of three stations with different mean temperature values (e.g. one station located at sea leve, one at 1000m asl and the third one at 2000m asl) and with station records having different lengths, the resulting average series will be positively biased when the coldest station has no data and negatively biased when the warmest station has no data. To avoid biases that could result from these problems, monthly temperature and precipitation series are reduced to anomalies (deviation from the mean for temperature and ratio for precipitation) from the period with best coverage (19712000). Because many stations do not have complete records for the 19712000 period, a gapfilling technique have been developed to estimate 19712000 averages from neighbouring records (see Brunetti et al., 2006). The station records converted into anomalies are then interpolated onto a regular grid. 
The radial term was realised with a gaussian weighting function with the following form: with where i runs along the stations and is the distance between the station i and the grid point (x,y). With this choice of the c parameter, we have weights of 0.5 for station distances equal to 1/4 from the grid point we want to calculate. is defined as the mean distance of one grid point from its next one obtained by increasing both longitude and latitude by one grid step (it is a sort of mean length of the grid mesh diagonal). For a grid resolution of 1 deg (as in this case) the parameter is about 130 km. The angular term accounts for the geographical separation among the sites with available time series. It has the following form: where is the angular separation of stations i and l with the vertex of the angle defined at grid point (x,y). The final weight is the product of the radial and the angular terms. Each grid point was calculated under one of the following conditions: i) a minimum of two stations at a distance lower than , or ii) a minimum of one station at a distance lower than . The grid value computation (once the above conditions were satisfied) was then performed by considering all stations within a distance of . 
The reason is as follows: The availability of station data is typically not sufficient to ensure an even distribution of stations throughout a network. But by averaging station anomalies within regions of similar size (grid boxes) and then calculating the average of all the grid box averages, a more representative regionwide anomaly can be calculated. This makes grid box averaging superior to simply taking the average of all stations in the domain. A network of 1000 stations could theoretically have 700 stations in the northern half of the domain and 300 stations in the southern half. A simple average of the stations could easily create a bias in the domainwide average to those stations in the north. 
REFERENCES
M. Brunetti, M. Maugeri, F. Monti, T. Nanni; 2006. Temperature and precipitation variability in Italy in the last two centuries from homogenized instrumental time series. International Journal of Climatology, 26, 345381. Venema V. K. C., O. Mestre, E. Aguilar, I. Auer, J. A. Guijarro, P. Domonkos, G. Vertacnik, T. Szentimrey, P. Stepanek, P. Zahradnicek, J. Viarre, G. MÃ¼llerWestermeier, M. Lakatos, C. N. Williams, M. J. Menne, R. Lindau, D. Rasol, E. Rustemeier, K. Kolokythas, T. Marinova, L. Andresen, F. Acquaotta, S. Fratianni, S. Cheval, M. Klancar, M. Brunetti, C. Gruber, M. Prohom Duran, T. Likso, P. Esteban, and T. Brandsma; 2012. Benchmarking homogenization algorithms for monthly data. Climate of the Past, 8, 89115, doi:10.5194/cp8892012. 