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JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 114, D00D09, doi:10.1029/2008JD011394, 2009

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ArticleDimming/brightening over the Iberian Peninsula: Trends insunshine duration and cloud cover and their relations withatmospheric circulation
Arturo Sanchez-Lorenzo,1 Josep Calbó,2 Michele Brunetti,3 and Clara Deser4
Received 31 October 2008; revised 7 February 2009; accepted 18 February 2009; published 24 April 2009.

[1] This study analyzes the spatial and temporal changes in sunshine duration (SunDu)

and total cloud cover (TCC) over the Iberian Peninsula (IP) and four subregions
during 1961–2004 using high-quality, homogenized data sets. The analyses confirm thatover most of the IP and in most seasons, SunDu and TCC variations are strongly
negatively correlated, with absolute values 0.8–0.9. Somewhat weaker correlations(0.5–0.6) are found in the southern portion of the IP in summer. A large discrepancy
between the SunDu and TCC records occurs from the 1960s until the early 1980s when the
SunDu series shows a decrease that it is not associated with an increase in TCC. This
negative trend or ‘‘dimming’’ is even more pronounced after removing the effects of TCC
via linear regression. Since the early 1980s, the SunDu and TCC residual SunDu series
exhibit an upward trend or ‘‘brightening.’’ In addition to the long-term dimming andbrightening, the volcanic eruptions of El Chichon and Mount Pinatubo are clearly evident
in the TCC residual SunDu record. The TCC and SunDu records over the IP are wellcorrelated with sea level pressure (SLP), with above normal TCC and below normal
SunDu corresponding to below normal SLP locally in all seasons. The TCC and SunDu
related SLP changes over the IP in winter and spring are part of a larger-scale north-south
dipole pattern that extends over the entire Euro-Atlantic sector. Other more regional
atmospheric circulation patterns, identified from rotated principal component analysis, arealso linked to TCC and SunDu variations over the IP. Finally and perhaps surprisingly, theTCC residual SunDu series exhibits a statistically significant relationship with aregional atmospheric circulation pattern during spring, summer, and autumn.
Citation: Sanchez-Lorenzo, A., J. Calbó, M. Brunetti, and C. Deser (2009), Dimming/brightening over the Iberian Peninsula: Trends
in sunshine duration and cloud cover and their relations with atmospheric circulation, J. Geophys. Res., 114, D00D09, doi:10.1029/
2008JD011394.

1. Introduction[2] Within the last few decades, considerable changes in
the physical climate system have been detected globally.
Many of these changes have been attributed, with a very
high confidence level, to anthropogenic influences [Solomon
et al., 2007]. The most studied variable, global mean nearsurface air temperature, has risen by 0.74 ± 0.18°C over thelast century (1906 – 2005), with a rate of warming over thelast 50 years (0.13 ± 0.03°C per decade) that is nearly twicethat for the last 100 years and has no precedents in the
instrumental records [Trenberth et al., 2007]. Therefore,
global warming is a phenomenon established with highconfidence, while other climate variables bring more uncer1
Group of Climatology, Department of Physical Geography, Universityof Barcelona, Barcelona, Spain.
2
Group of Environmental Physics, University of Girona, Girona, Spain.
3
Institute of Atmospheric Sciences and Climate, Italian National
Research Council (ISAC-CNR), Bologna, Italy.
4
National Center for Atmospheric Research, Boulder, Colorado, USA.

Copyright 2009 by the American Geophysical Union.
0148-0227/09/2008JD011394$09.00

tainties regarding their changes and responses to anthropogenic forcing. For example, there are still large uncertainties
about how clouds will respond to climate change, despite
important advances in understanding during recent years.
Consequently, cloud feedbacks are the primary source ofintermodel differences in equilibrium climate sensitivity,with low clouds being the largest contributor [Solomon etal., 2007].
[3] Clouds are the main cause of interannual and decadal
variability of radiation reaching the Earth’s surface andtherefore they exert a dominant influence on the global
energy balance. In fact, cloudiness can contribute to cooling,i.e., low-level clouds types linked to their high albedo [Maceet al., 2006], but also to warming, i.e., high clouds types emit
less radiation out to space than do low clouds or the clear
atmosphere [Lynch, 1996; Mace et al., 2006]. Regarding
climatic studies of cloudiness, a distinction must be madebetween studies based on ground level visual observations
and studies based on satellite data. A discussion about theadvantages and limitations of both sources of data are given
by Warren and Hahn [2002]. Although an accurate assessment of cloudiness variations on global or hemispheric scales

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can only be obtained through the use of satellite images,
climate analyses of such images is limited by the short periodof available data and also by calibration issues that undermine construction of homogeneous data sets required for
detecting climatic long-term trends.
[4] On the other hand, a widespread reduction of global
solar radiation between the 1950s and 1980s has been wellestablished and documented [e.g., Ohmura and Lang, 1989;
Gilgen et al., 1998; Stanhill and Cohen, 2001; Liepert,
2002], and since late 1980s a reversal in this trend has been
detected in many regions of the world [Pinker et al., 2005;
Wild et al., 2005]. This decrease and increase in surface
solar radiation have been defined as ‘‘global dimming’’ and‘‘global brightening,’’ respectively. Although causes of thisphenomenon are not fully understood currently, changes inthe transmissivity of the Earth’s atmosphere due to changes
in concentrations and optical properties of aerosols asconsequence of anthropogenic emissions are considered
the most likely causes [Stanhill and Cohen, 2001; Wild etal., 2005, 2007].
[5] However, both the global dimming and the recent
brightening carry uncertainty in their explanation and quantification as recently remarked the IPCC Fourth Assessment
Report [Trenberth et al., 2007, p. 279]. For example, somestudies found that the dimming period appears more clearlyin large urban areas as a consequence of local pollution andconsequently it might not be a global phenomenon [Alpert
et al., 2005; Alpert and Kishcha, 2008]. These studies also
pointed out the lack of stations with reliable and long-termseries of global radiation measurements in rural areas and in
nondeveloped countries. Since cloudiness is the largest
modulator of solar radiation reaching the ground, it has
also been suggested that the dimming period may be linked
to a detected increase in total cloud cover since the second
half of the 20th century over many regions in the world[Dai et al., 1999]. This increasing cloudiness since 1950 is
consistent with an increase in precipitation and a decrease
in daily temperature range [Vose et al., 2005]. In contrast,
a decrease in total cloud cover over land, from visualobservations and remote sensing [Rossow and Dueñas,2004; Warren et al., 2007], has been reported since the late1970s or the early 1980s; this cloudiness change can bereasonably related to the brightening period [Wild et al.,2005].
[6] However, it must be noted that during the dimming
period there were areas with decreasing cloudiness [e.g.,
Kaiser, 2000; Maugeri et al., 2001; Auer et al., 2007], andalso areas lacking cloud cover trends but decreases in solar
radiation reaching the surface [e.g., Stanhill and Moreshet,
1992; Stanhill and Cohen, 2001; Qian et al., 2006]. Also,
different studies have detected changes in global solar
radiation under clear skies [Abakumova et al., 1996; Wild
et al., 2005; Ruckstuhl et al., 2008] and cloudy skies[Liepert, 2002], presumably due to variations in atmospherictransparency linked to changes in anthropogenic aerosols.
Recent changes in emissions of the main anthropogenic
aerosols have been reported [Stern, 2006; Streets et al., 2006]
and may be partially responsible for the transition between
the dimming and brightening periods. Besides the direct
aerosol effect, i.e, aerosol capacity to scatter or absorb solar
radiation, it is important to consider as well the aerosol
indirect effects. These indirect effects are more uncertain

D00D09and correspond to aerosol induced changes in cloud properties such as lifetime and albedo, and have also been linked
to modification of precipitation forming processes [e.g.,
Ramanathan et al., 2001; Rosenfeld et al., 2008]. In fact,
since most IPCC climate models did not include the aerosol
indirect effects, it has been suggested that the agreement
between observed and simulated surface warming may bepartly spurious [Knutti, 2008].
[7] A difficulty in establishing causes of the global dimming and brightening is the limited number of solar radiation
series with accurate and calibrated long-term measurements.
For this purpose, the analysis should be supported andextended with the use of other climatic variables such as
evaporation, visibility, or sunshine duration (SunDu) records[Stanhill, 2005], especially with series starting before the1950s or in regions where solar radiation measurements are
not available. SunDu is defined as the amount of time, usually
expressed in number of hours, that direct solar radiation
exceeds a certain threshold (usually taken at 120 W m2).
Consequently, this variable can be considered as an excellent
proxy measure of global solar radiation on interannual [e.g.,
Iqbal, 1983; Stanhill, 2003] and also on decadal scales [e.g.,
Liang and Xia, 2005; Stanhill and Cohen, 2008], playing animportant role in the description of global dimming andbrightening phenomena.
[8] Moreover, an interesting way of investigating possible
explanations of interannual and decadal variability of radiation, SunDu, and/or cloudiness consists in analyzing theirrelationships to the atmospheric circulation patterns or‘‘teleconnections,’’ that normally are summarized by indicesthat simplify the spatial structure of pressure systems and thatcan be used as time series showing the evolution in amplitude
and phase of these modes of atmospheric variability [Hurrell
et al., 2003; Trenberth et al., 2007]. Many circulation patterns
or teleconnections have been identified for the Northern
Hemisphere that normally tend to be most prominent in
winter, when the mean circulation is stronger [e.g., Barnston
and Livezey, 1987; Hurrell et al., 2003]. Decadal variations in
the persistence of these circulation patterns can be associatedwith regional changes in different climatic variables, andconsequently during the last decades a growing interest has
been put on circulation patterns changes that may be indirectly related to the recent climate change of anthropogenic
origin [Solomon et al., 2007].
[9] The Iberian Peninsula (IP) is a region with few longterm solar radiation records [Norris and Wild, 2007]. However, a collection of 72 SunDu series over the IP has recently
been compiled and homogenized by Sanchez-Lorenzo et al.
[2007] (hereafter referred to as SL07). The resulting annual
SunDu series for the whole IP confirms a period of dimmingfrom the 1950s to the early 1980s, followed by a period ofbrightening until the end of the 20th century (SL07).
[10] In SL07, however, the role of cloudiness in SunDu
variability was not explored, despite the fact that it is wellknown that both variables are inversely related [e.g., Angell
et al., 1984; Angell, 1990; Jones and Henderson-Sellers,
1992]. Few studies on cloudiness climatology are published
for the IP or Spain; a recent work compared total cloud
cover (TCC) from different sources, and showed consistentdeclining trends for both reanalysis values (ERA-40) andremote sensing data (ISSCP) [Calbó and Sanchez-Lorenzo,
2009].

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SANCHEZ-LORENZO ET AL.: DIMMING/BRIGHTENING OVER IBERIA[11] Thus, the main objective of our study is to compare
high-quality data sets of SunDu and TCC series over the IP,
in order to determine the degree of agreement between bothvariables at different spatial and temporal resolutions,putting a special emphasis in detecting possible dimming/brightening subperiods over IP. The second objective is todetermine the main atmospheric circulation patterns over theEuro-Atlantic sector linked with SunDu and TCC variations
on interannual and decadal time scales. In section 2, we
describe the SunDu and TCC data sets and methods used inthis study. The annual and seasonal comparison of bothvariables is presented in section 3, and a residual SunDu
series is defined by removing the linearly associated TCC
variability. In section 4, the relationships between the TCC
and SunDu series and prominent atmospheric circulation
patterns are shown. Finally, conclusions of this paper arepresented in section 5.

2. Data Sets and Methods
2.1. Sunshine Duration and Cloudiness Data Sets
[12] The SunDu data set used here is the same that was
described and used in SL07, where details on the original
data, quality control checks, homogenization procedure, andgridding method can be consulted. The final data set is a
1° (latitude and longitude) resolution gridded version thatcovers the whole IP with 84 cells and complete records from1951 until 2004. For the present study we used the annual andseasonal series for the whole IP and 4 subregions obtainedby means of a Principal Component Analysis (PCA).
[13] The original cloudiness series used in this study wereobtained from the Spanish Agencia Estatal de Meteorologı́a(AEMET) formerly named Instituto Nacional de Meteorologı́a
and also from the Portuguese Instituto de Meteorologia. The
cloudiness database is constituted by 83 daily series of TCC
measured consistently in oktas, obtained from the average of
3-daily observations taken at 7, 13 and 18 UTC; all series areat least 30 years long and end in December 2004. Since
SunDu records integrate insolation during all daylight hours,
these 3 cloudiness observations per day seem adequate todefine a mean TCC that can be compared with SunDu series.
Following the recommendations of Aguilar et al. [2003] weapplied different quality control checks in order to (1) detectand correct/remove gross errors, such as aberrant (e.g., TCC
values greater than 8 oktas) or negative values; (2) remove
false zeros that can be an important source of error whenestimating the monthly mean; and (3) check the consistencyof calendar dates (days per year or month). Following thesequality control checks, the daily series were converted intomonthly values, by averaging the daily series of TCC inmonthly mean values. When more than 6 days in a month
were missing, we did not compute the monthly value, and thewhole month was set as missing.
[14] After obtaining the monthly series, we tested thehomogeneity of the TCC series. Note that these series canbring important inhomogeneities since are visual observations recorded by meteorological observers, so they arepartially subjective. Although there are many examples ofworks that apply homogenization procedures to different
climatic variables, such as temperatures or precipitation[e.g., see Aguilar et al., 2003, and references therein], few
studies have yet applied a homogeneity procedure on cloud-D00D09iness series. Maugeri et al. [2001] and Auer et al. [2007] aresome of the few exceptions: both works demonstrate that
TCC series are affected by temporal breaks that must be
corrected or eliminated before the assessment of long-termchanges in cloudiness. In the present work, the Craddock
relative homogeneity test [Craddock, 1979] was applied based
in a modification detailed by Brunetti et al. [2006] and SL07.
We rejected for the subsequent analyses 14 complete series
with many inhomogeneities, and we also removed several
subperiods of other series. Thus, the final monthly TCC data
set consists of 69 series across the whole IP (Figure 1).
Although there are some series with data starting in the 1930s,
there is a clear increase of data availability only after 1961.
Therefore, we limited the cloudiness and SunDu data sets to
the 1961– 2004 period.
[15] Then, all gaps between the first available year of eachseries and December 2004 were filled with estimates based
upon the highest correlated reference (neighboring) series.
Finally, we generated a gridded version for the TCC data setsin order to minimize possible errors resulting from eventuallypersistent inhomogeneities and to overcome problems related
to nonhomogeneous spatial coverage of the stations. We
followed the same interpolation technique described in
SL07 and the grid was constructed for the same domain(9°W – 3°E; 36°N–45°N), at the same 1° spatial resolution(Figure 1), and was calculated at monthly, seasonal, andannual resolution, on the basis of single station anomaly series(obtained as ratio to the corresponding 1971–2000 mean). The
reliability of these TCC gridded series was then confirmed
by comparison with daily temperature range data [SanchezLorenzo et al., 2008b]. Thus, TCC grid can be easily compared with SunDu data set since both variables used a similar
number of initial series and have been converted to the samegrid domain and spatial resolution using the same interpolation gridding technique.
2.2. SunDu and TCC Regionalization and Mean Series
Construction[16] Since we decided to study the spatial behavior ofdifferences between TCC and SunDu over the IP, we started
by establishing different subregions in the area. As in SL07
for the SunDu series, for the TCC data set the regionalization approach was based on a S-Mode PCA [Preisendorfer,
1988] that defines the main modes of temporal variability in
TCC over the IP. We applied the PCA to the gridded dataset, starting from the correlation matrix, and considering all
the 12 monthly anomalies of the year in order to obtain aunique regionalization and to avoid inconvenient seasonal
differentiation. Six of the obtained Empirical Orthogonal
Functions (EOF) have eigenvualues greater than 1, explaining
together near the 94% of the total variance in the data set.
Only the first four EOF, which have eigenvalues greater than2, were retained and a Varimax rotation was applied to thecorresponding eigenvector. The obtained regions are almost
identical to those obtained with the SunDu series (SL07,
Figure 5), and consequently we defined exactly the same 4
subregions in order to simplify the comparison between bothvariables. Summarizing the results, we identified 4 subregions which comprise the central-east (E), north (N), west(W) and southern (S) sectors of the IP. Subsequently, we
computed the TCC annual and seasonal mean series for thewhole IP and the 4 subregions as an arithmetic mean of

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D00D09Figure 1. Location of the 83 cloudiness series obtained for the IP, with indication of the 69 selected(black circles) and 14 rejected (white circles) stations after the homogenization procedure. The 84 gridcells generated with 1° of spatial resolution are indicated too.
the 84 grid cells and of the corresponding grid cells in each
subregion, respectively. This spatial averaging approachenhances the signal-to-noise ratio for better identificationof interannual and decadal variability in the data.
[17] The overall linear trends of all series in this paper
were calculated over the 1961– 2004 period by means ofleast squares linear fitting, and their significance estimatedby the Mann-Kendall nonparametric test at the 5% level ofconfidence. Also, all time series shown in this paper areplotted together with their 11-a window 3-a s Gaussian lowpass filter for a better visualization of long-term and decadal
variability.
2.3. Classification of Atmospheric Circulation Patterns
in the Euro-Atlantic Sector[18] The analysis of the circulation patterns was performedon seasonal mean sea level pressure (SLP) provided by the
National Center for Atmospheric Research (NCAR) on aregular 5°  5° grid [Trenberth and Paolino, 1980] (dataavailable at http://dss.ucar.edu/datasets/ds010.1). We selecteda window over the Euro-Atlantic sector (50°W – 40°E;
20°N –70°N) during the same 1961– 2004 period that covers
the SunDu and TCC series. We discarded the annual basis
analysis since there are important differences in the variability and modes of circulation patterns along the year [Barnston
and Livezey, 1987].
[19] Unrotated PCA in S-mode [Preisendorfer, 1988] wasapplied to the seasonal anomalies of SLP, using the correlation matrix in order to ensure the inclusion of the lower
variance in the lower latitudes of our domain [Barnston andLivezey, 1987]. Under the S-mode approach, clusters of grid
points with similar time behaviors are obtained by theprincipal component (PC) loadings, and the structure of
the time behavior is categorized by the PC scores. Thus, theobtained results can be interpreted as teleconnections or
atmospheric circulation patterns that capture the leading
modes of SLP variability [Huth, 2006]. We repeated theanalyses by using the covariance matrix and similar results
were obtained (not shown). The number of components tobe retained was determined from the eigenvalue versus PC
number plots (Scree Test), assuming that the convenient
choice is indicated by the end of a section with a small slopethat is followed by a pronounced drop [O’Lenic and Livezey,
1988]. Also, a minimum of 70% of the total explained
variance in the retained components [Briffa et al., 1994]
was required.
[20] Since unrotated S-mode PCA can produce artifacts in
the results, we rotated the retained components. The rotation
produces real physical patterns with more statistically robust
solutions [Huth, 2006], with a redistribution in the final
explained variance between the rotated components thatenables to a clearer separation of components and concentrates the loadings for each component into the most influential variables. We used the Varimax rotation which is themost widely applied and recommended option for circulation
pattern classification [Barnston and Livezey, 1987; Huth,
2006]. Subsequently, we estimated, by regression of theloadings for each rotated EOF, the PC time series (scores)that characterize the EOF time behavior during the analyzed
period.

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D00D09Figure 2. (left) Mean annual (top) SunDu and (bottom) TCC and (right) the corresponding mean
monthly course over the IP during the 1971 – 2000 period.
[21] We have also computed one-point correlation maps
between the SunDu (or TCC) series and the gridded SLPtime series for the 1961 –2004 period. The aim of theseanalyses is to give a more direct assessment of the role of
SLP variations in SunDu and TCC variability over the IP,
and also to verify the results based on PCA.

3. Sunshine Duration, Total Cloud Cover, andDimming/Brightening Trends
3.1. Spatial and Temporal Comparison of Sunshine
Duration and Cloudiness[22] Figure 2 shows the interpolated maps of the meanannual series of SunDu and TCC (left), with their mean
monthly course over the whole IP (right) for the 1971 – 2000
period. The annual SunDu and TCC maps show a similar
but opposite pattern and clear latitudinal dependence, with
SunDu (TCC) less (more) than 2000 h per year (4.5 oktas)
in the northern area and more (less) than 2800 h per year
(3.5 oktas) in the southern sectors of the IP. Besides thiszonal mean pattern there is a slight influence of the Atlantic
Ocean since SunDu (TCC) isolines indicate, for a given
latitude, lower (higher) values in the west compared to theeast. The mean seasonal cycles of SunDu and TCC are outof-phase. SunDu reaches maximum values during summer(more than 275 h per month during June, July, and August),
and minimum values in winter (less than 150 h per month
during November, December, January, and February). Thisis obviously related with the astronomical course of the Sun

in these latitudes, but it might be also influenced by varying
cloudiness. Indeed, TCC shows a minimum in summer,with less than 3 oktas in July and August, but there is not aclear maximum since several winter and spring months (fromOctober to May) reach more than 4 oktas. It is important tohighlight that SunDu annual mean is more influenced by thesummer than by the other seasons while the opposite is true
for TCC.
[23] Figure 3 shows the relationship between annual andseasonal SunDu and TCC anomalies for all IP cells during
the 1961 – 2004 period, and the linear regressions ofthese points are also shown to represent the mean behavior
of SunDu in relation with TCC. For the annual data
(Figure 3a), the correlation coefficient between the SunSu
and TCC is 0.54 (a  0.01). On the other hand, during
winter (Figure 3b) the correlation coefficient increases to0.88 (a  0.01), so an excellent fit between the values
exists. In addition, in winter most data are close to the
diagonal line. Meanwhile, for summer (Figure 3d) the
correlation coefficient decreases to 0.62 (although it isalso significant at the a  0.01 level). As in the annual
scatterplot, during summer the points do not fall symmetrically around the diagonal line. For spring (r = 0.79,
a  0.01 level) and autumn (r = 0.80, a  0.01 level) the
behavior is similar, but in an intermediate state between
winter and summer. The SunDu anomalies in excess ofthe expected values, in cases of high TCC anomalies, might
be related to the well-known tendency of ground-based

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D00D09Figure 3. Relationship between SunDu and TCC, where each point is the mean for 1 year’s data at one
grid point during the 1961 – 2004 period ((a) annual, (b) winter, (c) spring, (d) summer, and (e) autumn).
The values are expressed as relative deviations from the 1971 – 2000 mean and the linear regression isindicated in each plot.
observers to overestimate the TCC because of their inability
to detect fractional cloudiness when clouds have significant
vertical extent, a factor that is more important during summer
over the IP when most clouds are of convective origin insteadof frontal origin [Angell et al., 1984]. In contrast, when
SunDu anomalies are underestimated, for lower TCC anomalies, the cause may be related to atmospheric aerosols whichreflect and absorb solar radiation and reduce the amount of
direct solar radiation reaching the Earth’s surface [Stanhill,2003]. As shown in Figure 3, this phenomenon is especially
important during the summer, the period of the year
which shows the greatest aerosol concentrations over the IP[Papadimas et al., 2008].
[24] Figure 4 shows the local correlation coefficients
between SunDu and TCC over the IP based on annual andseasonal data, using interpolated values obtained at each grid

point. All correlation coefficients exceed the 95% significance level. For the annual map (Figure 4a), the greater
values in the northern sectors of the IP are in contrast with thelower correlations obtained in the southern areas. Note thatthe annual values are not representative for the whole year,
since for winter, spring, and autumn there are in generalgreater values (r > 0.8) for the whole IP. This indicates thata major part of the interannual variation in SunDu is probably
a result of cloudiness variations. On the other hand, insummer (Figure 5d) there is also high correlation in thenorthwestern sectors, but the values decrease clearly in thesouthern area. Consequently, SunDu variance explained by
TCC is lower, which may be related to the different nature(more convective and fractional) of summer cloudiness, orto the effect of higher aerosol concentrations (dust, smoke,
and/or haze) [Papadimas et al., 2008].

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D00D09is a clear dimming in SunDu while TCC remains relatively
constant. In this season we also detect a clear minimum in the
SunDu anomalies (1982 – 1984), which is not clearly marked
in the TCC series. As a consequence of these differences, thelinear trend for the whole analyzed period is not significant
for the SunDu series but there is a significant TCC decreaseof 2.2% per decade. This disagreement is enhanced during
summer, with a slight decrease in the correlation (r = 0.73)
and again a decrease in SunDu during the 1960 – 1980s
period that is not associated with an increase in TCC. Bothlinear trends show negative nonsignificant values. Finally, inautumn both series match quite well, similarly to the winterseries (r = 0.88). The subregional analysis show similar
results to the mean IP series following the spatial andtemporal signals detected in Figures 4 and 5.

Figure 4. Pearson’s correlation coefficient between SunDu
and TCC series during the 1961 – 2004 period ((a) annual,(b) winter, (c) spring, (d) summer, and (e) autumn). Absolutevalues greater than 0.40 are statistically significant at the 1%
level.

[25] Figure 5 shows the mean annual and seasonal time
evolution series for SunDu and TCC (with reversed axis) for
the whole IP. These mean series are significantly correlated,
as it was obtained from the scatterplots considering all grid
points (Figure 3). Thus, for the annual series (Figure 5a)there is a correlation of 0.60 (a  0.01); note howeverthat there is a clear disagreement between both series from the
1960s to mid-1980s. Thus, SunDu shows a clear decrease, or
dimming, during this subperiod while TCC shows a stabilization or slight decrease that does not match with the
behavior of SunDu. After the mid-1980s there is a good
agreement between both variables since SunDu (TCC)
increases (decreases) until 2000, and then show a new slightdecrease (increase) during the more recent years. Also, it isvery remarkable that the SunDu absolute minimum reachedin 1982 – 1984 does not correspond with high TCC anomalies(values are below the 1971 – 2000 mean). Regarding longterm trends over the 1961 – 2004 period, SunDu series showsa slightly negative, nonsignificant value, while for TCC there
is a significant decrease of 1.4% per decade.
[26] In winter (Figure 5b) the SunDu and TCC time series
match almost perfectly (r = 0.95), and, in contrast to theannual series, there is no disagreement between SunDu andTCC series during the first half of the analyzed period. Bothlinear trends over the 1961 – 2004 period are not significant.
During spring, there is a high correlation between SunDu
and TCC series (r = 0.87), but also a clear discrepancy
during the 1960– 1980 period: as in the annual series, there

3.2. Residual Anomalies Between SunDu and TCC[27] Summarizing the previous section, TCC variability
accounts for much of the SunDu variability over the IP oninterannual and decadal time scales. However, there is afraction of SunDu variability that cannot be explained by
TCC variability (especially during spring and summer), andother factors, such as changes in aerosol optical thickness(AOT), may be important to understand the variations ofsolar radiation reaching the surface. In fact, the variability in
AOT is relatively small in comparison to mean cloud optical
thickness values and variability; consequently, direct radiative forcing by aerosols is much lower in overcast than inclear sky conditions because the incoming solar radiation isscattered or absorbed by clouds instead of by aerosols[Norris and Wild, 2007]. In order to remove the cloud effectand detect a dimming or brightening signal linked to otherfactors, and similarly to other authors [e.g., Wild et al., 2005;
Norris and Wild, 2007] we obtained the residual series bysimply subtracting the expected SunDu (according the observed TCC anomalies) from the measured SunDu. Specifically, for the annual and seasonal basis, we used the linear
regressions showed in Figure 3 and then we subtracted the
expected SunDu anomalies from the observed SunDu
anomalies. In order to simplify the interpretation of theresults, we avoided possible subregional differences andthe residual series was obtained only for the whole IP. The
residual annual and seasonal time series are all significantly(a  0.01) correlated, with correlation coefficients greaterthan 0.70 except between spring and winter (r = 0.54) andspring and autumn (r = 0.64).
[28] The annual residual series for the whole IP shows aclear decrease from the 1960s to the beginning of the 1980s
with a subsequent recovery to the 2000s punctuated by two
distinct minima in 1982–1985 and in 1992–1993 (Figure 6a).
Thus, after removing the TCC effect, there is a clear decrease(increase) in SunDu anomalies during the first (last) two
decades that cannot be explained by TCC. The two pronounced minima are remarkable, and likely related to the
El Chichón (April 1982) and Pinatubo (June 1991) large
volcanic eruptions. In fact, it is well known that the global
effects of a large volcanic eruption are caused by droplets ofsulfuric acid that efficiently scatter shortwave radiation, inducing a decrease (increase) of the amount of direct (diffuse)solar radiation reaching the surface and leading to cooling[Robock, 2000]. The seasonal residual time series are similarin shape to the annual residual record (Figures 6b–6e). The

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D00D09Figure 5. Annual and seasonal time evolution of both SunDu (solid lines) and TCC (dashed lines)
series (thin lines) for the whole IP during the 1961 – 2004 period, plotted together with the 11-a window
3-a s Gaussian low-pass filter (thick lines; (a) annual, (b) winter, (c) spring, (d) summer, and (e) autumn).
The series are expressed as relative deviations (%) from the 1971– 2000 mean. Note that the scale for
TCC series has a reversed axis.

low values reached during 1982– 1984 are also noteworthy inall seasons although they are clearer during spring andsummer; the other minimum reached during 1992– 1993 isclear in all seasons but summer. Linear trends over the period
as a whole are negative and significant only in the winter andsummer series (similar results hold if the years 1982– 1984
and 1992 are eliminated from the analyses).
[29] A limitation in the previous residual anomalies series
is the difficulty in expressing the changes in suitable units.
Another limitation is related to the fact that the residual
series combine variations in clear sky solar radiation flux
with variations in cloud optical thickness that are unrelated
to cloud cover [Norris and Wild, 2007]. In order to confirm
the possibility of a direct aerosol effect in the residual series
we calculated the SunDu mean for clear sky conditions.
Since this analysis is based on daily data, we only selected thecompletely homogeneous series in both SunDu and TCC
variables and containing at least 30 years of data in daily

resolution during the 1961 – 2004 period. These restrictions
resulted in a selection of only 11 stations, which fortunately
are well distributed across the IP. In these series, a day wasdefined as clear if the mean TCC from the 3 daily observations is less than 1.5 oktas, following the criterion establishedby AEMET. The annual and seasonal mean IP series wereobtained by averaging the 11 SunDu anomalies (obtained as
differences to the corresponding 1971 – 2000 mean) series
expressed in hours per day, for the clear sky days selected ineach station. The mean IP annual SunDu for clear sky
conditions (Figure 7a) shows a decrease from the 1960s
to the beginning of the 1980s, with a minimum in 1983.
Afterward a positive trend appears up to the end of theanalyzed period, only interrupted by another relative minimum in 1992. The seasonal time series show positive
significant correlations (r  0.50, a  0.01) and a temporal
behavior that resembles the annual series, although for springand summer there is a more obvious minimum at the

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D00D09Figure 6. IP residual anomalies after removing the TCC effect in the SunDu series (thin line), plotted
together with the 11-a window 3-a s Gaussian low-pass filter (thick line), during the 1961 – 2004 period((a) annual, (b) winter, (c) spring, (d) summer, and (e) autumn). The series are expressed as relative
deviations (%) from the 1971 – 2000 mean.
beginning of the 1980s and a more constant decrease andincrease during the first and last two decades, respectively.
Finally, neither the annual nor the seasonal series show any
significant trend over the period of record. These mean IP
SunDu series under cloud free days were correlated with theresidual series, and consistently we found highly significant
correlations (r  0.65, a  0.01) both at annual and seasonalbasis.

4. SunDu and TCC Relationships With
Atmospheric Circulation Patterns[30] To assess the linkages between atmospheric circulation variations and TCC/SunDu changes, we have computed
one-point correlation maps between gridded SLP anomalies
over the Euro-Atlantic sector and the IP TCC and SunDu
series for each season separately (Figure 8). As expected,
the patterns and amplitudes of the SLP correlation maps arenearly equal and opposite for TCC and SunDu. Locally overthe IP, above (below) normal SLP is associated with below(above) normal TCC and above (below) normal SunDu inall seasons, consistent with synoptic experience. The local
SLP anomalies are part of a more extensive pattern in allseasons except summer. For example in winter, the SLP
correlation pattern consists of a zonally elongated northsouth dipole extending over the entire Euro-Atlantic domain
with a nodal line near 55°N. This pattern bears someresemblance to the NAO but it is shifted northward by
5 – 10° of latitude. A similar although spatially more
confined SLP dipole pattern occurs in spring and to a lesser
extent in autumn. The amplitudes of the SLP correlation
coefficients are generally greatest in winter (maximum
values 0.8) and smallest in summer (maximum values0.5), well in excess of the 0.05 significance value of 0.3.
In summary, interannual and decadal variations in TCC and
SunDu over the IP are associated with local changes in SLP

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D00D09Figure 7. Daily mean SunDu (hours) series over the IP for cloud-free sky conditions (thin line), plotted
together with the 11-a window 3-a s Gaussian low-pass filter (thick line; (a) annual, (b) winter, (c) spring,(d) summer, and (e) autumn). The series are expressed as daily SunDu anomalies (hours) from the 1971 –2000 mean.
in all seasons, and with anomalous large-scale atmosphericcirculation patterns in all seasons except summer. The
seasonal one-point SLP correlation maps based on theresidual SunDu record (not shown) are considerably weaker
than those based on the original TCC and SunDu records.
[31] Next, we examined the relationships between preferred patterns of atmospheric circulation variability and the
TCC/SunDu records over the IP. To determine the dominantpatterns of atmospheric circulation variability over theEuro-Atlantic sector, we applied a separate rotated PCA to
the gridded SLP anomalies in each season. The number of
EOFs retained in the rotated PCA (and their total varianceexplained) are four (82%) for winter, six (80%) for spring,eight (81%) for summer, and eight (85%) for autumn. We
then correlated the PC time series associated with eachrotated EOF with the SunDu, TCC, residual SunDu, and clear
sky SunDu time series for the whole IP and the four IP
subregions (Table 1). Only those EOFs that are significantly
correlated with SunDu or TCC are discussed.

[32] In winter, PC1 and PC4 are significantly correlated(a  0.01) with the SunDu (positive correlation) and TCC(negative correlation) series over the IP and over most of
the IP subregions. In its positive phase, EOF1 (Figure 9a) isdefined by high- and low-pressure systems over the Mediterranean basin and northern Europe, respectively. This
dominant mode of winter SLP variability has been detected
previously over a similar domain [Slonosky et al., 2000;
Rimbu et al., 2006], an aspect that contrasts with otheranalyses applied over greater domains where other modes(specifically, the North Atlantic Oscillation, NAO) aredetected as the leading mode of variability [Hurrell et al.,2003]. In fact, in our analyses, EOF2 (not shown) represents
the well-known spatial structure of the NAO, although witha westward displacement, and its PC series is not significantly correlated with either SunDu or TCC. However, bothrotated PC1 (r = 0.68) and PC2 (r = 0.56) are highly
correlated with the NAO index [Jones et al., 1997] indicatingthat both circulation patterns are regional manifestations

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D00D09Figure 8. Spatial distribution of correlations between SLP and the mean IP (top) SunDu and (bottom)
TCC series ((a and e) winter, (b and f) spring, (c and g) summer, and (d and h) autumn). The dashedcontours indicate approximate 95% significant levels (jrj  0.30, a  0.05).

of the NAO. These results help to reconcile the results basedon one-point SLP correlation maps (Figure 8a) and areconsistent with previous findings [Pozo-Vázquez et al.,
2004; Sanchez-Lorenzo et al., 2008a], that established ahighly significant positive correlation between the NAO andthe sunshine duration in southern Europe. PC4 (Figure 9c)
also shows significant correlations with SunDu and TCC,
except for the N subregion. During the positive phase of thiscirculation pattern there is anomalous high pressure over the
Atlantic Ocean centered north of the Azores islands. This
circulation pattern, which does not exhibit a dipole configuration, is not significantly correlated with the NAO index.

Finally, PC3 (Figure 9b) has significant (a  0.05) positive(negative) correlations with the SunDu (TCC) series only
for subregions N and W. This pattern shows a single-cellstructure centered over Central Europe which, during its
positive phase, is associated with anomalous easterly flow
over the IP. Under these conditions, while the eastern andsouthern regions of the IP receive humid air, the remaining
parts of the IP (west and north) are notably dry [LopezBustins et al., 2008]. In general, similar winter trends andatmospheric circulation influence in TCC can be observed forthe IP in the context of the whole Mediterranean basin andusing the data NCEP/NCAR reanalysis data set [Lolis, 2009].

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D00D09

Table 1. Correlation Coefficients Between the PC Time Series of Rotated SLP EOFs Over the Euro-Atlantic Sector and the Time Seriesof SunDu, TCC, SunDu Residual and SunDu Clear Sky Over the IP and the Four IP Subregionsa
SunDu
SLP EOFSLP %Variance

IP

E

N

TCC
W

S

IP

E

N

W

S

IP SunDu Residual

IP SunDu Clear Sky

.56
.62


.45
.41
.64

.58

.66



+





1
3
4

28.5
15.5
14.9

.52
+
.63

.50

.62

.52
.51
+

.38
.38
.65

.52

.59

Winter.57 .57

.65 .64

1
4

42.3
16.8

.69


.68


.72


.54


.62


Spring.64 .64



.65
+

.51


.61


+
.54

+
.44

2
5

26.6
20.7

.32
.53

.34
.45

+
.46

.36
.46

+
.44

Summer.45 .42
+
+

.48
.30

.51
.31


+

+
.54


.43

5
6
7

20.0
19.8
17.2

.33
.30
.51

+
.36
.46

.37



+

.50

+

.74

Autumn.43 .38++
.54 .47

.41
+


.37
+
.51

.42
+
.65


.42
+


.39


a

Only those EOFs that are significantly correlated with the SunDu and/or TCC records are shown. Correlation coefficients significant at a  0.01 (a 0.05) are shown in bold (italics); values with lower levels of significance are indicated by sign (+ or ) only.

Neither the residual nor the clear sky SunDu series exhibit
significant correlations with any of the winter SLP EOFs.
Regarding long-term trends, although EOF1 shows a slightly
increase, none of the three PC time series (Figure 9) has
significant trends.
[33] In spring, the leading EOF (Figure 10a) represents asimilar spatial structure as the leading EOF in winter, andconsequently can also be considered as a regional manifestation of the NAO. The PC series of this pattern shows
positive (negative) significant correlations (a  0.01) with
SunDu (TCC) series for the whole IP and all subregions.
Moreover, a clear increase of this pattern is detected from the
1980s, resulting in a positive significant trend over the
analyzed period. This significant positive increase agrees
with the significant decrease in TCC detected over the whole
IP. Similar to winter, EOF2 (not shown) represents the typical
NAO pattern configuration, with the Icelandic low and the
Azores high centers of action. But, as in winter, this patterndoes not have significant correlations with SunDu and TCC
series; the same is true for the remaining circulation patterns.
Another relevant result during spring is the significant
negative correlations (a  0.01) between PC4 (Figure 10b)and the residual (r = 0.52) and clear sky SunDu (r = 0.44)
series. The positive phase of this pattern is characterized bya single-cell high-pressure system over the central North
Atlantic Ocean (somewhat similar to the spatial configurationof winter EOF4, Figure 9c), which may be regarded as a
blocking situation. However, the physical connection between this pattern and the residual or clear sky series is notunderstood. In agreement with the residual and clear sky
SunDu series, PC4 shows a general upward trend from the
1960s to 1980s with a subsequent decrease to the present.
[34] During summer, the relationships between SunDu or
TCC and the dominant modes of atmospheric circulation
variability are generally weaker than in winter and spring.
This is understandable given that clouds have a more convective as opposed to dynamical origin in the warm season.
In summer, PC2 (Figure 11a) is most strongly correlated with
TCC while PC5 (Figure 11b) is most strongly correlated with

SunDU. In its positive phase EOF2 exhibits an anomalous
anticyclone centered over the Mediterranean basin which
promotes sunnier and less cloudy conditions. The positive
phase of EOF5 exhibits an anomalous anticyclone over the
Atlantic Ocean northwest of Africa, with an anticyclonicridge that extends northeastward up to the IP. This pattern issignificantly negatively correlated (a  0.01) with thesummer SunDu residual (r = 0.54) and clear sky SunDu(r = 0.43) records. As in spring with EOF4 (Figure 10b),
there is not a clear physical explanation for the connection
between this anomalous SLP pattern and the SunDu records.
PC5 shows an increase from the 1960s to 1980s, with atendency toward more negative phases during the last two
decades.
[35] In autumn, the strongest linkages between SunDu or
TCC and preferred atmospheric circulation patterns occurs
for PC7 (Figure 12c). The positive phase of this pattern ischaracterized by a high-pressure system over the southwestern
IP, which generates stable and fair weather conditions, consistent with the sign of the correlations in Table 1. Contrarily,during the negative phase there is a low-pressure system thatgenerates an important cyclogenesis with a southern flow overthe IP that invigorates convective cloudiness and rainfall. In
fact, EOF7 resembles the Western Mediterranean Oscillation(WeMO) identified by Martin-Vide and Lopez-Bustins [2006]
and is significantly correlated (r = 0.63, a  0.01) with the
WeMO index (http://www.ub.es/gc/English/wemo.htm). Also
PC5 (Figure 12a) exhibits significant (a  0.05) positive(negative) correlations with the IP SunDu (TCC) series. The
positive phase of this pattern exhibits an anomalous anticyclonic system over the central Mediterranean basin and thenorth part of Africa. The well-known impact of this type ofcirculation pattern [Escudero et al., 2005] is an increase in
African dust intrusions (increasing AOT) over the IP. This may
reduce the direct solar radiation down to values lower than thethreshold required to mark the sunshine duration recorder, thus
explaining the nonsignificant correlations with many of theregional SunDu series. Finally, the autumn PC6 (Figure 12b),
whose associated EOF resembles the spatial configuration of

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D00D09

D00D09Figure 9. (left) Three EOFs of the winter SLP anomalies over the Euro-Atlantic sector displayed as PC
loading. Negative loadings are dashed, the contour increment is 0.2, and the zero contour has been
excluded. (right) PC time series of each EOF (thin line), plotted together with the 11-a window 3-a s
Gaussian low-pass filter (thick line; (top) EOF1, (middle) EOF3, and (bottom) EOF4).

EOF5 in summer (Figure 11b), exhibits significant correlations
with the residual SunDu (r = 0.42, a  0.01) and clear sky
SunDu (r = 0.39, a  0.01) series. These results confirm therelationship between this mode of atmospheric circulation andthe dimming/brightening phenomena over the IP. The PC
series of this pattern, which does not have a significant trend
over the analyzed period, shows an increase in its positive
phase during the 1970s and early 1980s, with a decrease until
the end of the 20th century.

5. Conclusions[36] We have presented in this paper a spatial and temporalcomparison between sunshine duration and total cloud cover
over the Iberian Peninsula, on the basis of homogenized andgridded data sets obtained from about 70 instrumental series

covering the period 1961– 2004. We took special care to
reduce the inhomogeneities in the original data, since otherwise the partial subjectivity of conventional cloudinessobservations could have introduced important biases in the
final results, especially in long-term estimations.
[37] As in previous studies in different areas of the world[e.g., Angell, 1990; Jones and Henderson-Sellers, 1992], we
detected a negative and highly significant correlation between both variables, although lower correlations were found
for the spring and summer series, compared with winter orautumn data. In general, the correlations are lower in thesouthern sectors of the IP than in the north. On the basis of thelong-term comparison, it is clear that the most important
discrepancy between SunDu and TCC is detected from the
1960s until the early 1980s, particularly during spring andsummer; specifically, SunDu shows a clear decrease that is

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Figure 10. As in Figure 9 but in spring, and for two EOFs ((a) EOF1 and (b) EOF4).

Figure 11. As in Figure 9 but in summer, and for two EOFs ((a) EOF2 and (b) EOF5).
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D00D09Figure 12. As in Figure 9 but in autumn, and for three EOFs ((a) EOF5, (b) EOF6, and (c) EOF7).

not associated with an increase in TCC. Similar results havebeen demonstrated recently for northern Europe [Stjern et al.,2009].
[38] The computed residual SundDu series after removalof the cloudiness-related variability, and the residual clear
sky SunDu series, highlight the period of dimming from the
1960s to the early 1980s followed by a period of brightening
in the most recent decades. The dimming and brightening
detected here over the IP show clear resemblance with thatobtained for Central Europe from more sophisticated methods
and data sets [Norris and Wild, 2007] and might thus beregarded as a large-scale phenomenon. Thus, we consider
that the most likely causes for the decline and subsequent
recovery in the residual SunDu series and series of SunDu
under clear skies are related to changes in aerosol radiative
effects, corresponding with reported increases and decreasesof anthropogenic aerosols during the dimming and brightening
periods, respectively. Another remarkable feature in our
residual SunDu series is the strong minima reached during
1982–1984 and 1992– 1993, both in the annual and seasonalseries, which are likely related to aerosol emissions after the
El Chichón and Pinatubo volcanic eruptions. However, tocompletely reject the influence of clouds in the dimming/brightening phenomena over the IP, analysis of additional
cloudiness parameters besides TCC is needed (e.g., type,vertical distribution and optical thickness) [Sun et al., 2007].
[39] We have also shown that interannual and decadal
variability of TCC and SunDu over the IP are linked to an
NAO-like pattern of SLP variability, albeit with a slightnorthward and eastward shift. This association is strongest
during winter and weakest in summer. We have further
demonstrated that TCC and SunDu variations are linked to

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more regional patterns of atmospheric circulation variability
identified on the basis of rotated PCA. Surprisingly, we havealso detected significant correlations between particularregional atmospheric circulation patterns in spring, summer
and autumn and the residual SunDu and clear sky SunDu
records. These intriguing results may hint at the possibilityof an impact of anthropogenic aerosols emissions on the
dynamics of the atmospheric circulation at synoptic scales,and should be explored further.
[40] Acknowledgments. This research was supported by the Spanish
Ministry of Science and Innovation (MICINN) projects NUCLIER(CGL2004 – 02325) and NUCLIEREX (CGL2007 – 62664). Arturo SanchezLorenzo was granted an FPU predoctoral scholarship by the MICINN anddeveloped part of this work while performing research at the Institute ofAtmospheric Sciences and Climate, Italian National Research Council(ISAC-CNR, Bologna). The sunshine duration and cloudiness series were
provided by the AEMET (Spain) and Instituto de Meteorologia (Portugal).
We would like to thank the two anonymous reviewers for their usefulcomments. We also extend our sincere thanks to Martin Wild, Associate
Editor of this special issue, for his comments and encouragement.

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M. Brunetti, Institute of Atmospheric Sciences and Climate, Italian
National Research Council (ISAC-CNR), Via P.Gobetti 101, I-40129
Bologna, Italy.
J. Calbó, Group of Environmental Physics, University of Girona, Campus
Motivili ESP-II, E-17071, Girona, Spain.
C. Deser, National Center for Atmospheric Research, P.O. Box 3000,
Boulder, CO 80307-3000, USA.
A. Sanchez-Lorenzo, Group of Climatology, Department of PhysicalGeography, University of Barcelona, C/Montalegre n° 6, E-08001
Barcelona, Spain. (asanchezlorenzo@ub.edu)

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