All the assessment reports (AR) published by the Intergovernmental Panel of Climate Change (IPCC) show that there is overwhelming scientific evidence of the existence of global warming (GW). It is also well known that climate change (CC) is a non-uniform phenomenon. What is not so clear is the degree of heterogeneity across all the regions in our planet. In fact, an important part of the Sixth Assessment Report (AR6) published by the IPCC in 2021-2022 is dedicated to this issue: climate (warming) heterogeneity. This is reflected in the chapters studying regional climate change. Our paper introduces a new quantitative methodology that builds on that described in Gadea and Gonzalo 2020 (GG2020) to characterize, measure and test the existence of such climate change heterogeneity (CCH). This is done in three steps. First, we introduce a warming typology (W1, W2 and W3 ) based on the trending behavior of the quantiles of the temperature distribution of a given geographical location. Second, we define in a testable format the concepts of warming acceleration and warming amplification. These concepts help to characterize (more ordinally than cardinally) the warming process of different regions. And third, we propose the new concept of warming dominance (WD) to establish when region A suffers a worse warming process than region B. We have chosen Spain as a benchmark geographical location because, as the AR6 report states ". . . Spain is fully included in the Mediterranean (MED) Reference

Region, but is one of the most climatically diverse countries in the world. . . ". This fact opens up the possibility of studying warming heterogeneity (WH) from Spain to the Globe (outer heterogeneity, OWH) and also from Spain to some of its regions represented by Madrid and Barcelona (inner heterogeneity, IWH). The three steps rely on the results reported in GG2020, where the different distributional characteristics (moments, quantiles, inter quantile range, etc.) of the temperature distribution of a given geographical location are converted into time series objects. By doing this, we can easily implement and test all the concepts involved in the three steps. A summary of the results is as follows. Spain and the Globe present a clear warming process; but it evolves differently. Spain goes from a warming process where lower and upper temperatures share the same trend behavior (IQR is maintained constant over time, warming type W1 ) to one characterized by a larger increase in the upper temperatures (IQR increases over time, warming type W3 ). In contrast, the Globe as a whole maintains a stable warming type process characterized by lower temperatures that increase more than the upper ones (IQR decreases in time). 1 In our typology, this constitutes a case of warming type W2. Climate heterogeneity can go further. For instance, within Spain we find that Madrid is of type W3 while the warming process of Barcelona is of type W1. This is in concordance with the Madrid climate being considered a Continental Mediterranean climate while Barcelona is more a pure Mediterranean one. The proposed warming typology (W1, W2 and W3 ), although dynamic, is more ordinal than cardinal. In this paper, the strength of a warming process is captured in the second step by analyzing its acceleration and its amplification with respect to a central tendency measure of the temperature distribution. Acceleration and amplification contribute to the analysis of warming heterogeneity. The acceleration in the Globe is present in all the quantiles above q30 while in Spain it already becomes significant above the 10 th quantile. We find an asymmetric behavior of warming amplification; in Spain (in comparison with the Globe mean temperature) this is present in the upper temperatures (above the 80 th and 90 th quantiles) while in the Globe the opposite occurs (below the 20 th and 30 th quantiles). Within Spain, Madrid and Barcelona also behave differently in terms of acceleration and amplification. Overall, warming in Spain dominates that of the Globe in all the quantiles except for the lower quantile q05, and between Madrid and Barcelona there is a partial WD. Madrid WD Barcelona in the upper part of the distribution and Barcelona WD Madrid in the lower one. The existence of a clear heterogeneous warming process opens the door to the need of a new non-uniform causal (effect) research. One that goes beyond the standard causality in mean analysis (see Tol, 2021). CCH also suggests that in order for the mitigation-adaptation policies to be as efficient as possible they should be designed following a type of common factor structure: a common global component plus an idiosyncratic local element. This goes in the line with the results found in Brock

In this section, we briefly summarize the novel econometric methodology introduced in GG2020 to analyze Global and Local Warming processes. Following GG2020, Warming is defined as an increasing trend in certain characteristics of the temperature distribution. More precisely: Definition 1. (Warming): Warming is defined as the existence of an increasing trend in some of the characteristics measuring the central tendency or position (quantiles) of the temperature distribution. An example is a deterministic trend with a polynomial function for certain values of the β parameters

In GG2020 temperature is viewed as a functional stochastic process X = (X t (ω), t ∈ T ), where T is an interval in R, defined in a probability space (Ω, , P ). A convenient example of an infinite-dimensional discrete-time process consists of associating ξ = (ξ n , n ∈ R + ) with a sequence of random variables whose values are in an appropriate function space. This may be obtained by setting

so X = (X t , t = 0, 1, 2, ..., T ). If the sample paths of ξ are continuous, then we have a sequence X 0 , X 1 , .... of random variables in the space C[0, N ]. The choice of the period or segment t will depend on the situation in hand.
In our case, t will be the period of a year, and N represents cross-sectional units or higher-frequency time series. We may be interested in modeling the whole sequence of G functions, for instance the sequence of state densities (f 1 (ω), f 2 (ω), ..., f T (ω) ) as in Chang et al. (2015,   2016) or only certain characteristics (C t (w)) of these G functions, for instance, the state mean, the state variance, the state quantile, etc. These characteristics can be considered time series objects and, therefore, all the econometric tools already developed in the time series literature can be applied to C t (w). With this characteristic approach we go from Ω to R T , as in a standard stochastic process, passing through a G functional space:

Going back to the convenient example and abusing notation, the stochastic structure can be summarized in the following array:

The objective of this section is to provide a simple test to detect the existence of a general unknown trend component in a given characteristic C t of the temperature process X t . To do this, we need to convert Definition 1 into a more practical definition. Definition 2. (Trend test): Let h(t) be an increasing function of t. A characteristic C t of a functional stochastic process X t contains a trend if β = 0 in the regression

The main problem of this definition is that the trend component in C t as well as the function h(t) are unknown. Therefore this definition can not be easily implemented. If we assume that C t does not have a trend component (it is I(0)) 2 and 2 Our definition of an I(0) process follows Johansen (1995). A stochastic process Yt that satisfies

Ψ iz i converges for |z| < 1 + δ, for some δ > 0 and

, where the condition εt ∼ iid(0,σ 2 ) with σ 2 > 0 is understood. h(t) is linear, then we have the following well known result. Proposition 1. Let C t = I(0). In the regression

the OLS estimator

(5)

and asymptotically (T → ∞) t β=0 is N (0, 1). In order to analyze the behavior of the t-statistic t β = 0, for a general trend component in C t , it is very convenient to use the concept of Summability (Berenguer-Rico and Gonzalo, 2014) Definition 3. (Order of Summability): A trend h(t) is said to be summable of order "δ" (S(δ)) if there exists a slowly varying function L(T ), 3 such that

is O(1), but not o(1). Proposition 2. Let C t = h(t) + I(0) such that h(t) is S(δ) with δ ≥ 0, and such that the function g(t) = h(t)t is S(δ + 1). In the regression

the OLS β estimator satisfies

Assuming that the function h(t)

(See Embrechts et al., 1999, p. 564). Examples of how this proposition applies for different particular Data Generating Processes (DGP) can be found in GG. A question of great empirical importance is how our trend test (T T ) of Proposition 2 behaves when C t = I(1) (accumulation of an I(0) process). Following Durlauf and Phillips (1988), T

In the first model, z t is a fractional process with 1/2 < d < 3/2. In the second model, z t follows an AR, with its largest root close to unity, ρ T = 1 -c/T . In the third model, z t is decomposed into an I(1) and an I(0) component. Its simplest format is z t = υ t + t with υ t = υ t-1 +η t , where t is ID(0, q * σ 2 ), η t is ID(0, σ 2 ), σ 2 > 0 and both disturbances are serially and mutually independent. Note that the pure unit-root process is nested in all three models: d = 1, c = 0, and q = 0. The long-run properties implied by each of these models can be characterized using the stochastic properties of the partial sum process for z t . The standard assumptions considered in the macroeconomics or finance literature assume the existence of a "δ," such that T -1/2+δ T t=1 z t -→ σ H(. ), where "δ" is a model-specific constant and H is a model-specific zero-mean Gaussian process with a given covariance kernel k(r, s). Then, it is clear that the process C t = µ + z t is summable (see Berenguer-Rico and Gonzalo, 2014). This is the main reason why Proposition 3 holds for these three persistent processes. Proposition 3. Let C t = µ + z t , t = 1, ..., T , with z t any of the following three processes: (i) a fractional or long-memory model, with 1/2 < d < 3/2; (ii) a nearunit-root AR model; or (iii) a local-level model. Furthermore, T -1/2+δ T t=1 z t -→ σ H(. ), where "δ" is a model-specific constant and H is a model-specific zero-mean Gaussian process with a given covariance kernel k(r, s). Then, in the LS regression

After the development of the theoretical core, we are in a position to design tools to approach the empirical strategy. The following subsection describes each of them. From Propositions 2 and 3, Definition 2 can be simplified into the following testable and practical definition. Definition 4.
(Practical definition 2): A characteristic C t of a functional stochastic process X t contains a trend if in the LS regression,

Several remarks are relevant with respect to this definition: (i) regression (13)   has to be understood as the linear LS approximation of an unknown trend function White, 1980); (ii) the parameter β is the plim of β ols ; (iii) if the regression (13) is the true data-generating process, with u t ∼ I(0), then the OLS β estimator is asymptotically equivalent to the GLS estimator (see Grenander and Rosenblatt,   1957); (iv) in practice, in order to test β = 0, it is recommended to use a robust HAC version of t β=0 (see Busetti and Harvey, 2008); and (v) this test only detects the existence of a trend but not the type of trend. For all these reasons, in the empirical applications we implement Definition 4 by estimating regression (13) using OLS and constructing a HAC version of t β=0 (Newey and West, 1987). These linear trends can be common across characteristics indicating similar patters in the time evolution of these characteristics. all the slopes are equal,

This co-trending hypothesis can be tested by a standard Wald test. When m = 2 an alternative linear co-trending test can be obtained from the regression

.., m by testing the null hypothesis of β = 0 vs β = 0 using a simple

Climate classification is a tool used to recognize, clarify and simplify the existent climate heterogeneity in the Globe. It also helps us to better understand the Globe's climate and therefore to design more efficient global warming mitigation policies. The prevalent climate typology is that proposed by Köppen (1900) and later on modified in Köppen and Geiger (1930). It is an empirical classification that divides the climate into five major types, which are represented by the capital letters A (tropical zone), B (dry zone), C (temperate zone), D (continental zone), and E (polar zone). Each of these climate types except for B is defined by temperature criteria. More recent classifications can been found in the AR6 of the IPCC (2021, 2022) but all of them share the spirit of the original one of Köppen (1900). The climate classification we propose in this section is also based on temperature data and it has three simple distinctive characteristics:

• It considers the whole temperature distribution and not only the average

• It has a dynamic nature: it is based on the evolution of the trend of the temperature quantiles (lower and upper). • It can be easily tested Definition 6. (Warming Typology): We define four types of warming processes:

• W0: There is no trend in any of the quantiles (No warming). • W1: All the location distributional characteristics have the same positive trend (dispersion does not contain a trend)

• W2: The Lower quantiles have a larger positive trend than the Upper quantiles (dispersion has a negative trend)

• W3: The Upper quantiles have a larger positive trend than the Lower quantiles (dispersion has a positive trend). Climate is understood, unlike weather, as a medium and long-term phenomenon and, therefore, it is crucial to take trends into account. Notice that this typology can be used to describe macroclimate as well as microclimate locations. Most of the literature on Global or Local warming only considers the trend behavior of the central part of the distribution (mean or median). By doing this, we are losing very useful information that can be used to describe the whole warming process. This information is considered in the other elements of the typology W1, W2 and W3. This typology does not say anything about the intensity of the warming process and its dynamic. Part of this intensity is captured in the following definitions of warming acceleration and warming amplification. Definition 7. (Warming Acceleration): We say that there is warming acceleration in a distributional temperature characteristic C t between the time periods t 1 = (1, ..., s) and t 2 = (s + 1, ..., T ) if in the following two regressions:

the second trend slope is larger than the first one:

In practice, we implement this definition by testing in the previous system the null hypothesis β 2 = β 1 against the alternative β 2 > β 1 An alternative warming acceleration test can be formed by testing for a structural break at t = s. Nevertheless, we prefer the approach of Definition 7 because it matches closely the existent narrative on warming acceleration in the climate literature. Definition 8. (Warming Amplification with respect to the mean): We say that there is a warming amplification in distributional characteristic C t with respect the mean if in the following regression:

the mean slope is greater than one:

When the mean, mean t , and C t come from the same distribution, we name this "inner" warming amplification. Otherwise, the mean may come from an external environment and, in that case, we call it "outer" warming amplification. Both concepts, acceleration and amplification, introduce a quantitative dimension to the ordinarily defined classification. For example, the acceleration, which has a dynamic character, allows us to observe the transition from one type of climate to another. Amplification, on the other hand, makes it possible to compare the magnitude of the trends that define each type of climate. It should be noted that, although static in nature, it can be computed recursively at different points in time. In

β τ ≥ 0 for all 0 < τ < 1 and there is at least one value τ * for which a strict inequality holds. It is also possible to have only partial (W D). For instance, in the lower or upper quantiles. 3 The data

The measurement of meteorological information in Spain started in the eighteenth century. However, it was not until the mid-nineteenth century that reliable and regular data became available.
In Spain, there are four main sources of meteorological information: the Resumen Anual, Boletín Diario, Boletín Mensual de Climatología and Calendario Meteorológico. These were first published in 1866, 1893, 1940 and 1943, respectively. A detailed explanation of the different sources can be found in Carreras and Tafunell (2006). Currently, AEMET (Agencia Estatal de Meterología) is the agency responsible for storing, managing and providing meteorological data to the public. Some of the historical publications, such as the Boletín Diario and Calendario Meteorológico can be found in digital format in their respective archives for whose use it is necessary to use some kind of Optical Character Recognition (OCR) software. 5 In 2015, AEMET developed AEMET OpenData, an Application Programming Interface (API REST) that allows the dissemination and reuse of Spanish meteorological and climatological information. To use it, the user needs to obtain an API key to allow access to the application. Then, either through the GUI or through a programming language such as Java or Python, the user can request data. More information about the use of the API can be found on their webpage. 6 In this paper, we are concerned with Spanish daily station data, specifically temperature data. Each station records the minimum, maximum and average temperature as well as the amount of precipitation, measured as liters per square meter. The data period ranges from 1920 to 2019. However, in 1920 there were only 13 provinces (out of 52) who had stations available. It was not until 1965 that all the 52 provinces had at least one working station. Moreover, it is important to keep in mind that the number of stations has increased substantially from only 14 stations in 1920 to more than 250 in 2019. With this information in mind, we select the longest span of time that guarantees a wide sample of stations so that all the geographical areas of peninsular Spain are represented. For this reason, we decided to work with station data from 1950 to 2019. There are 30 stations whose geographical distribution is displayed in the map in Figure 1. The original daily data are converted into monthly data, so that we finally work with a total of 30x12 station-month units corresponding to peninsular Spain and, consequently, we have 360 observations each year with which to construct the annual distributional characteristics. In the case of the Globe, we use the database of the Climate Research Unit (CRU) that offers monthly and yearly data of land and sea temperatures in both hemispheres from 1850 to the present, collected from different stations around the world. 7 Each station temperature is converted to an anomaly, taking 1961-1990 as the base period, and each grid-box value, on a five-degree grid, is the mean of all the station anomalies within that grid box. This database (in particular, the annual temperature of the Northern Hemisphere) has become one of the most widely used to illustrate GW from records of thermometer readings. These records form the blade of the well-known "hockey stick" graph, frequently used by academics and other institutions, such as, the IPCC. In this paper, we prefer to base our analysis on raw station data, as in GG2020. The database provides data from 1850 to nowadays, although due to the high variability at the beginning of the period it is customary in the literature to begin in 1880. In this work, we have selected the stations that are permanently present in the period 1950-2019 according to the concept of the station-month unit. In this way, the results are comparable with those obtained for Spain. Although there are 10,633 stations on record, the effective number fluctuates each year and there are only 2,192 stations with data for all the years in the sample period, which yields 19,284 station-month units each year (see this geographical distribution in the map in Figure 1). 8 In summary, we analyze raw global data (stations instead of grids) for the period 1950 to 2019, compute station-month units that remain all the time and with these build the annual distributional characteristics. In this section we apply our three-step quantitative methodology to show the existent climate heterogeneity between Spain and the Globe as well as within Spain, between Madrid and Barcelona. Because all our definitions are written in a testing format, it is straightforward to empirically apply them. First, we test for the existence of warming by testing the existence of a trend in a given distributional characteristic. How common are the trends of the different characteristics (revealed by a co-trending test) determine the warming typology. Second, the strength of the warming process is tested by testing the hypothesis of warming acceleration and warming amplification. And third, independently of the warming typology, we determine how the warming process of Spain compares with that of the Globe as a whole (we do the same for Madrid and Barcelona). This is done by testing for warming dominance. (17); and finally, we compare the CC of different regions, for Spain and the Globe, and within Spain, between Madrid and Barcelona, with our warming dominance test (see 18). 9

The cross-sectional analysis is approached under two assumptions. First, choosing a sufficiently long and representative period of the geographical diversity of the Spanish Iberian Peninsula, 1950-2019. Second, we work with month-station units from daily observations to construct the annual observations of the time series object from the data supplied by the stations, following a methodology similar to that carried out for the whole planet in GG2020. 10 The study comprises the steps described in the previous section. The density of the data and the evolution of characteristics are displayed, respectively in Figures 2 and3. We find positive and significant trends in the mean, max, min and all the quantiles. Therefore from definition 1, we conclude there exists a clear local warming (see Table 1).
The recursive evolution for the periods 1950-2019 and 1970-2019 shows a clear increase in the trends of the mean, some dispersion measures and higher quantiles (see the last column of Table 1). More precisely, there is a significant trend acceleration in most of the distributional characteristics except the lower quantiles (below q20 ). These quantiles, q05 and q10, remain stable. The co-trending tests for the full sample 1950-2019 show a similar evolution of the trend for all the quantiles with a constant iqr (see Table 2). This indicates that in this period the warming process of Spain can be considered a W1 type. More recently, 1970-2019, the co-trending tests (see Table 3) indicate the upper quantiles grow faster than the lower ones. This, together with a positive trend in the dispersion measured by the iqr shows that Spain has evolved from a W1 to a 9 Before testing for the presence of trends in the distributional characteristics of the data, we test for the existence of unit roots. To do so, we use the well-known Augmented Dickey-Fuller test (ADF; Dickey and Fuller, 1979), where the number of lags is selected in accordance with the SBIC criterion. The results, available from the authors on request, show that the null hypothesis of a unit root is rejected for all the characteristics considered. 10 The results with daily averages are very similar. The decision to work with monthly data instead of daily in the cross-sectional approach has been based on its compatibility with the data available for the Globe. Finally, no evidence of "inner" amplification during the period 1950-2019 is found in the lower quantiles. Regarding the upper quantiles, we found both "inner" and "outer" amplification in the second period, which supports the previous finding of a transition from type W1 to type W3 (see Table 4). Summing up, with our proposed tests for the evolution of the trend of the whole temperature distribution, we conclude that Spain has evolved from a W1 type to a much more dangerous W3 type. The results of acceleration and dynamic amplification reinforce the finding of this transition to type W3. Note: OLS estimates and HAC p-values of the t-statistic of testing H0 : βi = 1 versus Ha : βi > 1 in the regression: Cit = βi0 + βi1meant + it. mean refers to the average of the Spanish Global temperature distribution for the "inner" and "outer"cases, respectively. In this section, we carry out a similar analysis to that described in the previous subsection for Spain. Figures 4 and5 show the time evolution of the Global temperature densities and their different distributional characteristics from 1950 to 2019. The data in both figures are obtained from stations that report data throughout the sample period. Table 5 shows a positive trend in the mean as well as in all the quantiles. This indicates the clear existence of Global warming, more pronounced (larger trend) in the lower part of the distribution (a negative trend in the dispersion measures). The warming process suffers an acceleration in all the quantiles above q30. From the co-trending analysis (see Tables 6 and7) we can determine the type of warming process characterizing the whole Globe. Table 6 indicates that in the period 1950-2019 the Globe experimented a W2 warming type (the lower part of the temperature distribution grows faster than the middle and upper part, implying iqr and std have a negative trend). Similar results are maintained for the period 1970-2019 (in this case only the dispersion measure std has a negative trend). The asymmetric amplification results shown in Table 8 reinforce the W2 typology for the whole Globe: an increase of one degree in the global mean temperature increases the lower quantiles by more than one degree. This does not occur with the upper part of the distribution. Notice that this amplification goes beyond the standard Artic amplification (q05 ) affecting also q10, q20 and q30. Summing up, the results from our different proposed tests for the evolution of the trend of the whole temperature distribution indicate that the Globe can be cataloged as a undergoing type W2 warming process. This warming type may have more serious consequences for ice melting, sea level increases, permafrost, CO 2 migration, etc. than the other types. Note: Annual distributional characteristics (quantiles) of temperature. The top panel shows the Wald test of the null hypothesis of equality of trend coefficients for a given set of characteristics. In the bottom panel, the TT is applied to the difference between two representative quantiles. Note: Annual distributional characteristics (quantiles) of temperature. The top panel shows the Wald test of the null hypothesis of equality of trend coefficients for a given set of characteristics. In the bottom panel, the TT is applied to the difference between two representative quantiles. Note: OLS estimates and HAC p-values of the t-statistic of testing H0 : βi = 1 versus Ha : βi > 1 in the regression: Cit = βi0 + βi1meant + it. mean refers to the average of the Global temperature distribution. The goal of this section is to show the existence of climate heterogeneity by comparing the results obtained from applying our three-step methodology to different regions. These results are summarized in Table 10. It is clear that there is distributional warming in all the analyzed areas; but this warming follows different patterns and sometimes the warming type is not even stable. In the case of Spain, it depends on the period under consideration. Figure 6 captures graphically the different trend behavior and intensity of the distributional characteristics by regions (Spain and the Globe and Madrid and Barcelona). 13 The graphical results in this figure coincide with the results of the warming typology tests shown in Table 10. The middle of Table 10 shows that warming acceleration is detected in all the locations. This acceleration is more general in Spain than in the Globe (see also the heatmap in Figure 7) and in Barcelona than in Madrid.
Apart from these differences, the acceleration shares certain similarities across regions. This is not the case for the warming amplification that is clearly asymmetric. Spain suffers an amplification in the upper quantiles while the Globe does so in the lower ones. Notice that the latter amplification goes beyond the standard results found in the literature for the Arctic region (q05 ). We detect amplification also for the regions corresponding to the quantiles q10 -q30. In the case of Madrid and Barcelona, Madrid suffers a wider warming amplification than Barcelona. The results of the first two steps of our methodology are obtained region by region (Spain, the Globe, Madrid and Barcelona). It is the last step, via the warming dominance test (see the numerical results in Table 9) where we compare directly one region with another. Warming in Spain dominates that of the Globe in all the quantiles except the lower q05. 14 This would support the idea held in European institutions and gathered in international reports on the greater intensity of climate 13 The analysis of other characteristics such as the third and fourth order moments can contribute to the temperature distributions. In the case of Spain, the kurtosis is always negative with a mean value of -0.8 and a significant negative trend, which means that we are dealing with a platykurtic distribution with tails less thick than Normal, a shape that is accelerating over time. However, it is ot possible to draw conclusions about symmetry given its high variability over time. Conversely, the temperature distribution in the Globe is clearly leptokurtic with an average kurtosis of 0.9 and a negative but not significant trend. The global temperature observations are therefore more concentrated around the mean and their tails are thicker than in a Normal distribution. The skewness is clearly negative although a decreasing and significant trend points to a reduction of the negative skewness. 14 A more detailed analysis of the warming process suffered in the Artic region can be found in Gadea and Gonzalo (2021). change in the Iberian Peninsula. Warming in Madrid dominates that of Barcelona in the upper quantiles, while the reverse is the case in the lower quantiles. This latter result coincides with the idea that regions close to the sea have milder upper temperatures. Further research (beyond the scope of this paper) will go in the direction of finding the possible causes behind the warming types W1, W2, and W3. Following the literature, on diurnal temperature asymmetry (Diurnal Temperature Range = DT R = T max -T min ) we can suggest as possible causes for W2 the cloud coverage (Karl et al. 1993) and the planetary boundary layer (see Davy et al. 2017). For W3, the process of desertification (see Karl et al. 1993). Summarizing, in this section we describe, measure and test the existence of warming heterogeneity in different regions of the planet. It is important to note that these extensive results can not be obtained by the standard analysis of the average temperature. The existence of Global Warming is very well documented in all the scientific reports published by the IPCC. In the last one, the AR6 report (2022), special attention is dedicated to climate change heterogeneity (regional climate). Our paper presents a new quantitative methodology, based on the evolution of the trend of the whole temperature distribution and not only on the average, to characterize, to measure and to test the existence of such warming heterogeneity. It is found that the local warming experienced by Spain (one of most climatically diverse areas) is very different from that of the Globe as a whole. In Spain, the upper-temperature quantiles tend to increase more than the lower ones, while in the Globe just the opposite occurs. In both cases the warming process is accelerating over time. Both regions suffer an amplification effect of an asymmetric nature: there is warming amplification in the lower quantiles of the Globe temperature (beyond the standard well-known results of the Arctic zone) and in the upper ones of Spain. Overall, warming in Spain dominates that of the Globe in all the quantiles except the lower q05. This places Spain in a very difficult warming situation compared to the Globe. Such a situation requires stronger mitigation-adaptation policies. For this reason, future climate agreements should take into consideration the whole temperature distribution and not only the average. Any time a novel methodology is proposed, new research issues emerge for future investigation. Among those which have been left out of this paper (some are part of our current research agenda), three points stand out as important:

• There is a clear need for a new non-uniform causal-effect climate change analysis beyond the standard causality in mean. • In order to improve efficiency, mitigation-adaptation policies should be designed containing a common global component and an idiosyncratic regional element. • The relation between warming heterogeneity and public awareness of climate change deserves to be analyzed. Note: OLS estimates and HAC p-values of the t-statistic of testing H0 : βi = 1 versus Ha : βi > 1 in the regression: Cit = βi0 + βi1meant + it. mean refers to the average of the Barcelona or Spanish temperature distribution for the "inner" and "outer"cases, respectively. Definition 9. (Warming Dominance (WD): We say that the temperature distributions of Region A warming dominates (W D) the temperature distributions of Region B if in the following regression

Note: OLS estimates and HAC p-values in parenthesis of the t β=0 test from regression: C t = α + βt + u t , for two different time periods. For the acceleration hypothesis we run the system: C t = α 1 + β 1 t + u t , t = 1, ..., s, ..., T, C t = α 2 + β 2 t + u t , t = s + 1, ..., T, and test the null hypothesis β 2 = β 1 against the alternativeβ 2 > β 1 .
We show the value of the t-statistic and its HAC p-value. Note: Annual distributional characteristics (quantiles) of temperature. The top panel shows the Wald test of the null hypothesis of equality of trend coefficients for a given set of characteristics. In the bottom panel, the TT is applied to the difference between two representative quantiles. Note: OLS estimates and HAC p-values in parenthesis of the t β=0 test from regression: C t = α + βt + u t , for two different time periods. For the acceleration hypothesis we run the system: C t = α 1 + β 1 t + u t , t = 1, ..., s, ..., T, C t = α 2 + β 2 t + u t , t = s + 1, ..., T, and test the null hypothesis β 2 = β 1 against the alternativeβ 2 > β 1 . We show the value of the t-statistic and its HAC p-value. Note: OLS estimates and HAC p-values in parenthesis of the t β=0 test from regression: C t = α + βt + u t , for two different time periods. For the acceleration hypothesis we run the system: C t = α 1 + β 1 t + u t , t = 1, ..., s, ..., T, C t = α 2 + β 2 t + u t , t = s + 1, ..., T, and test the null hypothesis β 2 = β1 against the alternativeβ 2 > β1. We show the value of the t-statistic and its HAC p-value. Similar results for Central England are found in GG2020 and for the US in Diebold and Rudebush

, 2022. This definition is slightly different from the one in Carrion-i-Silvestre and Kim (2019). In the CRU data there are 115 Spanish stations. However, after removing stations not present for the whole 1880 to 2019 period, only Madrid-Retiro, Valladolid and Soria remain. Since 1950, applying the same criteria, only 30 remain. From Madrid and Barcelona there is data since 1920's, nevertheless we began the study in 1950 for consistency with the previous analysis of Spain and the Globe. See the application to Central England in GG2020 and inGadea and Gonzalo (2022) to Madrid, Zaragoza and Oxford.