Systematic Correlation Matrix Evaluation (SCoMaE) – a bottom–up, science-led approach to identifying indicators
- 1Geography, Planning, and Environment, Concordia University, Montréal, QC, Canada
- 2GEOMAR Helmholtz Centre for Ocean Research Kiel, Department of Marine Biogeochemistry, 24105 Kiel, Germany
- 3Kiel University, 24098 Kiel, Germany
- aformerly at: GEOMAR Helmholtz Centre for Ocean Research Kiel, Department of Marine Biogeochemistry, 24105 Kiel, Germany
Correspondence: Nadine Mengis (email@example.com)
This study introduces the Systematic Correlation Matrix Evaluation (SCoMaE) method, a bottom–up approach which combines expert judgment and statistical information to systematically select transparent, nonredundant indicators for a comprehensive assessment of the state of the Earth system. The methods consists of two basic steps: (1) the calculation of a correlation matrix among variables relevant for a given research question and (2) the systematic evaluation of the matrix, to identify clusters of variables with similar behavior and respective mutually independent indicators. Optional further analysis steps include (3) the interpretation of the identified clusters, enabling a learning effect from the selection of indicators, (4) testing the robustness of identified clusters with respect to changes in forcing or boundary conditions, (5) enabling a comparative assessment of varying scenarios by constructing and evaluating a common correlation matrix, and (6) the inclusion of expert judgment, for example, to prescribe indicators, to allow for considerations other than statistical consistency. The example application of the SCoMaE method to Earth system model output forced by different CO2 emission scenarios reveals the necessity of reevaluating indicators identified in a historical scenario simulation for an accurate assessment of an intermediate–high, as well as a business-as-usual, climate change scenario simulation. This necessity arises from changes in prevailing correlations in the Earth system under varying climate forcing. For a comparative assessment of the three climate change scenarios, we construct and evaluate a common correlation matrix, in which we identify robust correlations between variables across the three considered scenarios.
An indicator is a quantitative value, measured or calculated, that describes relevant aspects of the state of a defined system. A useful indicator should fulfill certain characteristics that depend on the purpose of the indicator (Gallopín, 1996). Environmental indicators are developed based on quantitative measurements or statistics of environmental conditions in order to allow for a comparison of states of the environment across time or space (Ebert and Welsch, 2004). For environmental indicators of climate change Radermacher (2005) defined statistical measurability, political and societal relevance, and scientific consistency, i.e., a scientifically meaningful link between indicator and the state to be described, as the three main characteristics that should be considered as important during the indicator selection process. Moreover, other characteristics can be defined as desirable for such indicators, such as a high signal-to-noise ratio of the measurement, the relevance for ethical considerations, or the fact that the indicators chosen should not provide redundant information.
For the assessment of ongoing climate change, models representing the physical and biogeochemical processes of the Earth system and known as Earth system models (ESMs) are one of the essential tools because the inertia of the climate system to (carbon) perturbations requires projections of future climate states. Early climate models applied simple zero- to two-dimensional calculations to assess the effect of atmospheric CO2 on the climate by using global mean surface air temperature (SAT) as an indicator (Arrhenius, 1896; Callendar, 1938; Sellers, 1969). This commonly used climate change indicator, SAT, fulfills all three abovementioned characteristics. Several long-term temperature records as well as proxies for assessing SAT exist, which makes this indicator well measured (Statistical measurability). SAT is closely linked to other climate variables, e.g., evaporation, sea level rise, or biological productivity. Although SAT may not be the most relevant variable for society, using this indicator as a proxy for climate impacts is scientifically consistent (Seneviratne et al., 2016). Its political, economical, and ethical relevance evolved over time and is now evident in discussions concerning, e.g., global warming (Ott et al., 2004) or the 2∘ temperature increase target, which was endorsed by the Conference of the Parties in 2015 (UNFCCC, 2015). Working group II of the Intergovernmental Panel on Climate Change (IPCC) (Houghton et al., 2001) used SAT as the main climate change indicator, due to its predominance in the existing literature and its large scientific consistency as such.
But as Earth system models and observational data sets continuously increase in complexity, there are more and more variables available that could potentially serve as indicators of the state of the climate system. Which ones should we select for a fully comprehensive assessment of changes in the climate system, ideally, without providing redundant information? A common bottom–up approach for measuring complex systems is to start from a broad set of (Earth system) variables and consecutively select more appropriate ones depending on the research question (e.g., Kopfmüller et al., 2012; Pintér et al., 2005). For science-led climate change assessments reports, such as published by Working Group I of the IPCC, in addition to SAT, nowadays more indicators are selected to evaluate changes in different components of the Earth system, e.g., precipitation or often precipitation extremes, Arctic summer sea ice, or the rate of ocean acidification. Therefore, they are discussed in, e.g., the IPCC's summary for policy makers of the recent assessment report of climate change (Stocker et al., 2013).
The selection of a limited number of indicators that support scientific or political decision making is a major challenge for experts, who in this case have to decide on the relative importance of a variable in relation to others (Rametsteiner et al., 2011). There exist no unambiguous rules for the selection process (Böhringer and Jochem, 2007). Any indicator selection or metrics construction from Earth system variables implies a value and weighting decision and applies a weight of 0 to any disregarded variable. While the value judgment ideally requires the inclusion of potential end users or stakeholders, the weighting requires a well-informed and broad participation of scientific disciplines, i.e., expert judgment (Radermacher, 2005). However, selecting one indicator, while disregarding the other is a normative choice (Krellenberg et al., 2010), which can (unknowingly) be biased by, e.g., technical knowledge (Rametsteiner et al., 2011). Furthermore, Rametsteiner et al. (2011) point out that the ad hoc defined indicators should be subject to reevaluation over time.
In this study we want to introduce a bottom–up indicator selection method that uses statistical information about variables in addition to expert judgement, thereby attempting to reduce bias in the selection process. Systematic Correlation Matrix Evaluation (SCoMaE) uses information on correlations between variables to identify “clusters” of variables that show similar behavior. We then systematically select scientifically consistent indicators to represent these clusters. The identified indicators are independent and do not provide redundant information. A set of independent indicators hence allows for a more comprehensive science-led assessment of the system under consideration than a set of correlated indicators. Furthermore, SCoMaE allows for a learning process by providing new information about correlations between the given variables and hence increases the system understanding.
To illustrate the SCoMaE method, we exemplarily select indicators to answer the following research question: “How are changes in the climate system influenced by the sensitivity of the marine and terrestrial biological system to temperature and CO2?” This example application enables us to (1) illustrate how a correlation matrix can be constructed given a specific research question, (2) identify a comprehensive indicator set, (3) show that an indicator set derived from a certain forcing scenario is not necessarily appropriate to assess a changed forcing scenario, (4) identify a common indicator set valid for multiple forcing scenarios, and finally (5) illustrate how the method could be used in an iterative process including expert judgment or previous knowledge of the given system. These steps will serve as the guideline of this paper.
Before the SCoMaE method can be applied, it is crucial to identify and formulate the research question. For our example we chose to address the following research question: “How are changes in the climate system influenced by the sensitivity of the marine and terrestrial biological system to temperature and CO2?” While for this question we chose to evaluate perturbed parameter simulations of an intermediate-complexity Earth system model (see Sect. 2.1 and 2.3 for details), it is possible to apply this method to other data sets to answer different questions. Here are a few examples of alternative ways to define research questions and use the SCoMaE method to investigate them.
Our application is comparable with a multi-model ensemble where each of the perturbed parameters is a slightly different version of the default model. We could hence do the very same analysis as described in Sect. 3, with, e.g., the different models and scenarios simulated in the Coupled Model Intercomparsion Project 5 (CMIP5). The research question of how simulated changes in the climate system are influenced by multi-model model variability under climate change could be answered by this setting.
To select indicators to answer the research question of which changes in the simulated Earth system are robust throughout state-of-the-art Earth system models, we could again use the CMIP5 data sets. Here, one would probably want to calculate correlations between time series of different variables. This would give information about similar frequencies of those variables, which in turn suggests similar underlying processes. One could compare correlation matrices of one model during different forcing scenarios, as described in Sect. 3.3 and 3.4, or check the robustness of the correlations in one time period across models.
In that sense SCoMaE could also be applied to calculate correlations of observational time series. Since there is a higher level of noise within this data, it is possible to concentrate the research question on predefined timescales and filter the time series of the variables before applying the SCoMaE method. The indicators would accordingly be selected to answer the following underlying research question: “Which are the independent processes that I need to study for a comprehensive assessment of changes in the climate system of a given frequency band?”
Coming back to our example application of the SCoMaE method, we now want to briefly explain the model setup and simulations.
2.1 Model description
This paper illustrates the SCoMaE method for the example of model simulations performed with version 2.9 of the University of Victoria Earth System Climate Model (UVic ESCM), an Earth system model of intermediate complexity (Eby et al., 2013). It includes schemes for ocean physics based on the Modular Ocean Model Version 2 (MOM2) (Pacanowski, 1995), ocean biogeochemistry (Keller et al., 2012), and a terrestrial component including soil and vegetation dynamics (Meissner et al., 2003). It is coupled to a thermodynamic sea ice model (Bitz et al., 2001) with elastic visco-plastic rheology (Hunke and Dukowicz, 1997). The atmosphere is represented by a two-dimensional atmospheric energy moisture balance model (Fanning and Weaver, 1996). All model components have a common horizontal resolution of 3.6∘ longitude and 1.8∘ latitude and the oceanic component has a vertical resolution of 19 levels, with vertical thickness varying from 50 m near the surface to 500 m in the deep ocean. Wind velocities used to calculate the advection of atmospheric heat and moisture as well as the air–sea-ice fluxes of surface momentum and heat and water fluxes, are prescribed as monthly climatological wind fields from NCAR/NCEP reanalysis data (Eby et al., 2013). Wind anomalies, which are determined from surface pressure anomalies with respect to preindustrial surface air temperature, are added to the prescribed wind fields.
A list of the globally aggregated output variables is given in Table A1.
2.2 Spin-up and scenario forcing
For the default model simulation, the UVic ESCM was spun-up with preindustrial (year 1765) seasonal forcing for over 10 000 years. All simulations were integrated from 850 until 2005 using historical fossil-fuel emissions and land-use changes, as well as radiative forcing from solar variability and volcanic activity following Eby et al. (2013). Following Keller et al. (2014), continental ice sheets were held constant to facilitate the experimental setting and analyses. Warming from black carbon, indirect ozone effects, and cooling from indirect sulfate aerosol effects were not included. From 2005 onward until 2100 the Representative Concentration Pathway (RCP) 4.5 and 8.5 scenarios from Meinshausen et al. (2011) were implemented as an intermediate and high-CO2 emissions driven scenario, respectively.
For the sensitivity analysis performed with the UVic ESCM, different model input parameters and parameterizations were perturbed, and for some of them it was necessary to do a new model spin-up to reach steady-state conditions again; apart from this the forcing was the same for all simulations.
2.3 Parameter perturbations
In the following sections, the single-parameter perturbation experiments, which are used in the example and shown in Fig. 1, are explained in detail. We chose these parameters to explore the sensitivity of the UVic ESCM to uncertainties in terrestrial and marine biological productivity with respect to temperature and CO2, since these processes will influence the future carbon cycle. In addition, we perturbed ocean vertical diffusivity, since this is a physical process influencing marine carbon uptake. All parameters were perturbed within physically meaningful ranges, which were evaluated based on their agreement with the time series of the historical global mean air temperature (Fig. S5). See Table 1 for a quick overview of the simulations.
2.3.1 Vertical ocean diffusivity
Small-scale physical mixing (vertical diffusivity or diapycnal mixing) in the ocean is parameterized in all global models because of their resolution. Thus, this important process, which plays a key role in determining ocean circulation and biogeochemical cycles as well as ocean to atmosphere heat and carbon fluxes, is set by necessity as a single global value or several regional values that fall within the range of observational estimates of vertical diffusivity. To test how this affects all model results, we varied this parameterization by increasing and decreasing it by 50 % (Kv low and Kv high), which is within the range of observational estimates (Duteil and Oschlies, 2011). For this sensitivity analysis, the model was spun-up with the corresponding setting for 10 000 years until a new equilibrium climate state was reached.
2.3.2 Lower bounds of biological temperature sensitivity
Although biological processes are known to be sensitive to temperature, there is a significant amount of uncertainty in how biology will respond to warming caused by climate change (Friedlingstein et al., 2006; Taucher and Oschlies, 2011). Furthermore, there are many different ways to model the effects of temperature on biology, and it is not know which is best for Earth system model applications. To investigate the lower bounds of the sensitivity of biological processes to direct temperature effects, we conduct simulations where direct temperature effects on biology are not included. In order to ensure that global biogeochemical fluxes are as close to present-day ones as possible, flux-weighted global averages for temperature-dependent rates were set for all temperature-dependent functions (see Taucher and Oschlies, 2011 for details). This approach was applied separately to marine and terrestrial ecosystems:
No marine biological sensitivity to temperature: the results of this analysis can be used to estimate a lower boundary for how marine plankton and how their effect on biogeochemical cycles will respond directly to global warming (no marine T sens.). For this sensitivity analysis, the model was spun-up with the corresponding setting for 10 000 years until a new equilibrium climate state was reached.
No terrestrial vegetation sensitivity to temperature: the results of this analysis can be used to estimate a lower boundary for how terrestrial vegetation and its effect on the carbon cycle will respond directly to global warming (no terr. T sens.). For this sensitivity analysis, the model was spun-up with the corresponding setting for 10 000 years until a new equilibrium climate state was reached.
2.3.3 Vegetation and soil sensitivity to temperature
To further investigate the sensitivity of terrestrial biology to temperature, we varied the vegetation and soil Q10 values, which are observationally derived coefficients that are used to model the biological system rate of change in response to a 10 ∘C temperature increase. Low and high Q10 values of 1.5 and 3.0 (model default is 2.0), which are within the range of observational estimates (Lloyd and Taylor, 1994), were set to investigate how different terrestrial biological sensitivities to temperature affect the model results (veg. q10 low/high and soil q10 low/high). For this sensitivity analysis, the model was spun-up with the corresponding setting for 10 000 years until a new equilibrium climate state was reached.
2.3.4 CO2 fertilization of vegetation
Increasing atmospheric CO2 is thought to stimulate terrestrial carbon uptake through the process of CO2 fertilization (Keenan et al., 2013; Matthews, 2007). This negative carbon cycle feedback results in reduced atmospheric CO2 concentrations and has likely accounted for a substantial portion of the historical terrestrial carbon sink (Friedlingstein et al., 2006). However, the future strength of CO2 fertilization in response to continued carbon emissions is highly uncertain. In order to test the impact of this uncertainty for future climate change simulations, we followed the approach of Matthews (2007) by scaling the CO2 sensitivity of the terrestrial photosynthesis model. We performed a simulation with no CO2 fertilization effect (CO2 fert. zero), as well as two simulations where we varied the strength of the CO2 fertilization effect by increasing and decreasing it by 50 % (CO2 fert. high/low) relative to the default model. No additional model spin-up was needed since the simulated CO2 fertilization effect only happens when the atmospheric CO2 concentration begins to increase, e.g., from the preindustrial period onward.
2.3.5 CO2 sensitivity of transpiration
Transpiration by plants is highly sensitive to increases in atmospheric CO2, since plants tend to open their stomata less often in higher-CO2 environments in order to reduce water loss to the atmosphere. The strength of this effect and its impacts on climate are highly uncertain and have been studied both through observations and models (Keenan et al., 2013; Mengis et al., 2015; Van Der Sleen et al., 2014). To test how strongly this affects simulations of future climate, the amount of transpiration for all plant functional types was scaled after Mengis et al. (2015). In this approach the CO2 fertilization effect is not changed. Three simulations were performed: for the first simulation, transpiration did not change relative to the preindustrial level (transp. CO2 sens. zero); for the other two simulations, the scaled transpiration was increased and decreased by 50 % of the amount that the model would simulate with the default setting (transp. CO2 sens. high/low) as CO2 changes. No additional model spin-up was needed, since the effect of changing CO2 on transpiration only becomes evident when the atmospheric CO2 concentration begins to increase, e.g., from the preindustrial period onward.
2.3.6 Stoichiometric changes in response to changing ocean carbonate chemistry
Mesocosm studies that artificially increase the amount of CO2 in seawater (e.g., climate change experiments) have suggested that the C : N content of marine plankton may be sensitive to changes in carbonate chemistry. The mesocosm study of Riebesell et al. (2007) suggested that as CO2 increases, the C : N content of phytoplankton may increase, which is a change that would affect the amount of carbon exported to the deep ocean by biological processes and have an effect on other marine biogeochemical cycles. To test how this affects all model results, we implemented the mesocosm-derived relationship between the atmospheric CO2 concentration and the C : N content of plankton as in Oschlies et al. (2008) (CN CO2 sens.). No additional model spin-up was needed, since the effect of changing CO2 on plankton stoichiometry only becomes evident when the atmospheric CO2 concentration begins to increase, e.g., from the preindustrial period onward.
3.1 Step 1: calculate the correlation matrix
Throughout this study, a variable is defined as a model output or observational time series, whereas we refer to it as an indicator if a variable was selected to represent a certain aspect of the considered system. To obtain a comprehensive, nonredundant set of indicators to describe a given system, the first step is to construct a correlation matrix, i.e., a matrix including the correlation information of all the relevant Earth system variables to each other. The construction of the correlation matrix strongly depends on the research question and needs to be adjusted accordingly. The selection of which variables are the relevant variables for the given research question and hence should be included in the matrix, as well as the choice of how the correlations should be calculated is very important for the outcome of the study. In the same way, it is important to consider a reasonable signal-to-noise ratio within the data set chosen. Correlations could for example be calculated between time series of variables or their derivatives, absolute temporal changes, or spatial patterns. Alternatively, output from ensemble simulations could be used to calculate correlations between changes in variables due to the different ensemble members. The matrix is then evaluated based on the significance information of these correlations (see Step 2). Note that for this preselection of the possibly relevant variables to answer the given question, as well as for the construction of the correlation information in the matrix, a certain level of expert judgement is needed.
To illustrate the construction of the matrix based on our example simulations, we show how the correlation between changes in global mean “surface air temperature” (A_sat) and “Northern Hemisphere sea ice area” (O_iceareaN) in the Representative Concentration Pathway (RCP) 8.5 emission scenario (Meinshausen et al., 2011) due to the parameter perturbations translates to the corresponding correlation matrix entry (Fig. 1). In our example we want to study the correlations between changes in model output variables, induced by varying poorly constrained model input parameters concerning the carbon cycle. In the following we will refer to these as “correlation of variable changes”.
Assuming that the signal of interest is of a similar kind as the state differences between the start and the end of a climate change simulation, we start by calculating the temporal differences between 2005–2015 and 2090–2100 from a number of parameter perturbation simulations that serve as our ensemble in this example (see Sect. 2.3 for explanations of the parameter perturbations). This enables us to learn whether the different output variables show a similar behavior for the respective parameter perturbation. Then the Pearson correlation coefficients between these changes are calculated and tested by performing a two-sided test at a 5 % significance level, with N = 16, the number of perturbed parameter simulations, and accordingly tcrit = 2.145.
In our example, there is a negative correlation of variable changes evident between “surface air temperature” (A_sat) and “Northern Hemisphere sea ice area” (O_iceareaN). This illustrates that these model output variables show consistent opposite reactions towards the parameter perturbations, i.e., if the perturbation causes surface air temperatures to increase, it also causes northern hemispheric sea ice to decrease. This information is then written into the correlation matrix. By studying the constructed correlation matrix and studying single correlations of changes between model output variables, we can learn about basic processes within the simulated climate system and test whether these agree with our expectations. To simplify the visual analysis of our example we sorted the variables in the matrices according to their strength in correlation of variable changes relative to changes in the commonly used climate change indicator, i.e., “surface air temperature” (A_sat) in the historical scenario.
3.2 Step 2: cluster identification and indicator selection
To obtain a set of indicators for the assessment of changes in the system under consideration, we systematically evaluate the previously constructed correlation matrix (see Fig. 2 for an illustration of this procedure). To obtain a comprehensive, nonredundant indicator set, we follow these steps: (1) the first indicator is the variable with the highest number of significant correlations with other variables; (2) all variables with a significant correlation are clustered under this indicator; (3) these clustered variables are then excluded from the selection of the next indicator; (4) the next indicator is again the variable with the highest number of significant correlations with all the remaining variables; (5) this indicator selection procedure is repeated until all variables are clustered and are represented by an indicator. If a variable is not significantly correlated to any of the remaining variables, this variable is considered to be a single indicator. These single indicators are needed for a fully comprehensive assessment, since they show different behavior from all previously selected indicators and hence provide additional information.
In our example, we applied the SCoMaE method to the correlation matrix concerning 46 commonly used variables for the assessment of climatic changes in the historical forcing scenario, simulated by the UVic ESCM (see Sect. 2.1 for details on the simulations). We find that the first indicator for our research question in the historical period is “precipitation over ocean areas” (F_precipO) (Figs. 3 and S5). By following the respective column of F_precipO (17th from the right) in the correlation matrix, we can see that changes in this model output variable are significantly correlated to changes in all variables that are also significantly correlated to changes in “surface air temperature” (A_sat; first from the bottom), with the exception of “mean ocean temperature” (O_temp, 16th from the bottom) but in addition also link changes in global and terrestrial precipitation and evapotranspiration (F_precip, F_precipL and F_evap, F_evapL, respectively; 35th and 37th from the bottom) as well as changes in “surface net upward longwave radiation” (F_uplwr, 40th from the bottom). The changes in these variables due to parameter perturbations are not significantly correlated to changes in “surface air temperature” (A_sat). Hence, based on purely statistical considerations, using “precipitation over ocean” (F_precipO) as an indicator for the research question in the historical period would be preferable to global mean “surface air temperature” (A_sat), the main ad hoc indicator of historical climate change, since it potentially holds more information.
“Surface albedo on land” (A_albsurL) is identified as the second indicator. After excluding all variables correlated to changes in “precipitation over ocean” (F_precipO), its changes due to the parameter perturbations are significantly correlated to changes in “net surface downward shortwave radiation” (F_dnswr), “ocean oxygen” (O_o2), and “sea surface salinity” (O_salsur). The third indicator is “ocean surface alkalinity” (O_alksur), which shows the same response to the parameter perturbations as “ocean surface phosphate concentrations” (O_po4sur). When excluding all variables that are clustered under one of the three abovementioned indicators, three variables remain unclustered: “mean ocean temperature” (O_temp), “maximum meridional overturning” (O_motmax), and “ocean phytoplankton” (O_phyt). These variables are hence single indicators, which are needed for a comprehensive assessment of the system under consideration (Fig. 3b).
See Sect. 1 and Figs. S1 and S2 in the Supplement for the results of these analyses for the intermediate–high (RCP4.5) and the business-as-usual (RCP8.5) scenarios, respectively.
3.3 Step 3 (optional): comparison of indicators for the different forcing scenarios
In order to learn how well the previously identified indicators for one scenario explain a different scenario with changed forcing, we prescribe the use of the previously identified indicator set. The SCoMaE accordingly first uses these indicators and then analyses whether and which additional indicators are needed for a fully comprehensive assessment of the new scenario.
For the example, we prescribed the indicators identified for the historical scenario to assess the intermediate–high (RCP4.5) and the business-as-usual (RCP8.5) emission scenarios (Fig. 4). The results show that if we were to only utilize the indicators from the historical scenario for the assessment of the two RCP scenarios, we would not be able to assess all changes in the climate system as represented by our model: for the RCP4.5 scenario, we would obtain additional information by considering the variables “net top-of-atmosphere radiation” (F_netrad) and “ocean surface heat flux” (F_heat), which are clustered together, and “net upward longwave radiation” (F_uplwr) and “ocean surface salinity” (O_salsur), which form another indicator cluster (Fig. 4).
Note that Earth system variables clustered under the prescribed indicators differ among the different scenarios (compare Figs. 3 and S1): in the historical scenario the indicator “precipitation over ocean” (F_precipO) includes the output variables “net top-of-atmosphere radiation” (F_netrad), “ocean surface heat flux” (F_heat), “ocean surface nitrate” (O_no3sur), “top-of-atmosphere outgoing longwave radiation” (F_outlwr), and “net upward longwave radiation” (F_uplwr), all of which are not included in the “precipitation over ocean” (F_precipO) indicator of the RCP4.5 scenario. Instead, the indicator “precipitation over ocean” (F_precipO) for the RCP4.5 scenario includes “mean ocean temperature” (O_temp), which it is not included for the historical scenario.
The differences between the correlation matrices for the RCP8.5 scenario compared to the historical scenario are even larger (compare Figs. 3 and S2). For the RCP8.5 scenario, 8 out of 46 considered variables would not be included if we applied the indicators identified for the historical scenario. Instead we need three additional indicators for the assessment of the system under consideration, namely “net top-of-atmosphere radiation” (F_netrad), “ocean surface dissolved inorganic carbon” (O_dicsur), and “net surface downward shortwave radiation” (F_dnswr) (Fig. 4). Note that six of the eight remaining variables that were initially included in the first indicator cluster for the historical scenario, namely “precipitation over ocean” (F_precipO), are no longer significantly correlated to it for the RCP8.5 scenario.
These differences in the correlation matrices for the different forcing scenarios indicate changes in prevailing correlations between Earth system variables with the imposed climate forcing. This illustrates that a reevaluation of the indicators chosen may be needed for a comprehensive assessment of different climate strategies yielding different climate states.
3.4 Step 4 (optional): evaluation of a common correlation matrix
To advance this analysis such that changes in correlation matrices from different forcing scenarios can be taken into account, it is possible to create a correlation matrix representing only those correlations that are significant in all forcing scenarios; this is defined as a common correlation matrix. Applying the SCoMaE method to such a common correlation matrix identifies an indicator set that can be used to assess and also compare multiple scenarios and which hence differs from the previously identified sets for the individual correlation matrices.
To obtain a common indicator set for the three example forcing scenarios (historical, RCP4.5, and RCP8.5), we construct a correlation matrix in which only correlations of variable changes that are significant in all these scenarios are considered (Fig. 5). Furthermore the color shading indicates in which of the scenarios the correlations between variable changes were found to be significant.
A first visual evaluation of the common correlation matrix shows more reddish than bluish shading, which indicates that the correlation patterns for the historical and RCP4.5 scenarios are more similar than for the historical and RCP8.5 scenarios (Fig. 5). This means that for a lower future emission scenario, the indicators from the historical scenario are more suitable than for a higher future emission scenario. This is true with the exception of the terrestrial and oceanic carbon fluxes (F_carba2l and F_carba2o, respectively). These two fluxes are perturbed by the land-use scheme implemented in the RCP4.5 scenario, since this scenario includes a high amount of afforestation and reforestation. Furthermore, greenish shading shows correlations of variable changes that are significant only in the RCP scenarios, indicating that those correlations of variable changes depend on the increasing anthropogenic (mainly CO2) forcing, included only in these scenarios.
The first indicator obtained from the common SCoMaE analysis is “atmospheric CO2” (A_co2), which was also found to be the first indicator in the RCP8.5 scenario (Figs. S7 and S8). Its changes are significantly correlated to changes in 27 other output variables in all three scenarios. This indicates that these correlations of variable changes are robust throughout the different strength of CO2 forcing in the three scenarios. The fact that “atmospheric CO2” (A_co2) is the first indicator with a large number of correlated variables suggests its ability to reflect the changes in other Earth system variables with regard to the parameter perturbations, such as changes in temperatures, carbon fluxes, and moisture fluxes over the ocean. This can possibly be explained by the fact that the changes in these variables are sensitive to the imposed CO2 forcing, which in turn is reflected in the atmospheric carbon concentration.
The second indicator is “precipitation over land” (F_precipL), which is clustered with “terrestrial evapotranspiration” (F_evapL) and “net upward longwave radiation” (F_uplwr) (Fig. S6). This cluster accordingly represents changes in terrestrial moisture fluxes and the resulting surface upward fluxes of longwave radiation. The latter relates to the surface air temperature, which on land is strongly influenced by the amount of evapotranspiration, and the resulting evaporative cooling. Note that the fact that terrestrial moisture fluxes are clustered under a separate indicator suggests a different sensitivity of these variables to the perturbed parameters. Since these three variables show significant correlations of variable changes to each other in all three scenarios, one could use any of them as the indicator for this cluster. The same is true of the next indicators and their clusters, which are “air-to-sea carbon flux” (F_carba2o) and “soil respiration” (L_soilresp); “net top-of-atmosphere radiation” (F_netrad) and the “ocean surface heat flux” (F_heat); and “net surface downward shortwave radiation” (F_dnswr) and the “land surface albedo” (A_albsurL).
The remaining single indicators are “air-to-land carbon flux” (F_carba2l), “ocean surface nitrate” (O_no3sur), “top-of-atmosphere outgoing longwave radiation” (F_outlwr), “ocean oxygen” (O_o2), “ocean surface alkalinity” (O_alksur), “ocean phytoplankton” (O_phyt), “sea surface salinity” (O_salsur), “ocean surface phosphate” (O_po4sur), and “maximum ocean meridional overturning” (O_motmax).
3.5 Step 5 (optional): including expert judgment
If stakeholders or experts were to inform the indicator selection process, it would be possible to prescribe indicators and then use the SCoMaE analysis to identify additional uncorrelated variables that are needed to obtain a comprehensive assessment of the system. Also, instead of using global mean time series, one could look at time series of regions or already processed variables, such as heat stress or cumulative emissions. This approach in combination with the SCoMaE analysis enables us to learn about variables which have previously been disregarded but potentially provide new information about the system or to learn which of the indicators previously considered actually provide redundant information.
How would the common indicator set from our example change if we were to include the condition that surface air temperature should be the first indicator, instead of atmospheric CO2?
Prescribing “surface air temperature” (A_sat) as the first indicator for the common correlation matrix leads to the replacement of “precipitation over land” (F_precipL) by “precipitation over ocean” (F_precipO) as the second indicator (Fig. 5b); its change with the parameter perturbations is correlated with 12 variables that are clustered under this indicator. Almost all of these variables were initially clustered under “atmospheric CO2” (A_co2) but are not significantly correlated to changes in “surface air temperature” (A_sat). These variables mainly describe global and oceanic moisture fluxes, as well as carbon fluxes or reservoirs on land: “precipitation over the ocean” (F_precipO), “global evaporation” (F_evap), “global precipitation” (F_precip), “vegetation net primary productivity” (L_vegnpp), “leaf area index” (L_veglai), “vegetation carbon” (L_vegcarb), and the “surface upward sensible heat flux” (F_upsens). The only exception to this behavior is “total ocean carbon” (O_totcarb), which in turn becomes a single indicator. In addition the second indicator, “precipitation over the ocean” (F_precipO), now incorporates the previously identified clusters of the second and third indicators, namely the clusters of “precipitation over land” (F_precipL) and the “air-to-sea carbon flux” (F_carba2o). Only “net upward longwave radiation” (F_uplwr), which was also clustered under “precipitation over land” (F_precipL) becomes a single indicator, remaining unclustered when “surface air temperature” (A_sat) is prescribed as the primary indicator. In turn, “air-to-land carbon flux” (F_carba2l), which was a single indicator in the default SCoMaE analysis, is now clustered under “surface air temperature” (A_sat).
The third and fourth indicators are “net top-of-atmosphere radiation” (F_netrad) and “net surface downward shortwave radiation” (F_dnswr), which were found with the same underlying clusters in the default analysis (compare Figs. S8 and S9). Finally, eight of the nine previously identified single indicators remain unclustered and hence are still single indicators.
Although the total number of indicators has not changed, the identified clusters and their meaning differ: in the default analysis, the first indicator represented changes in temperatures, carbon fluxes, and global and oceanic moisture fluxes. If “surface air temperature” (A_sat) is prescribed, the global and oceanic moisture fluxes are moved to the second cluster, which in addition incorporates some Earth system variables from the previously identified second and third indicators. This is one example showing how the SCoMaE method allows for the inclusion of expert judgment or preconditions, is able to account for changes in correlation patterns, and allows one to determine which indicators are needed for a comprehensive and nonredundant assessment. (For more discussions, see Sect. 2 and Fig. S3 in the Supplement.)
4.1 Discussion of the results from the example
4.1.1 What were we able to learn from the example?
As illustrated above, the SCoMaE method statistically evaluates the correlations between changes in model output variables and uses this information to cluster variables, while selecting a representative indicator for each cluster. The example analyses of the individual scenarios illustrates the dependence of the indicator selection on the imposed forcing scenario. These results demonstrate that for our model, it is insufficient to apply the historical indicator set to the future scenarios with either higher CO2 forcing such as in the RCP8.5 scenario or more limited CO2 forcing and reduced anthropogenic land use such as in the RCP4.5 scenario. Although our analysis is too limited to conclusively determine a best set of climate change indicators in a purely scientific bottom–up approach, our results do suggest that a comprehensive assessment of future climatic states needs a reevaluation of the ad hoc indicators chosen, due to changes in prevailing climate responses.
We demonstrate one possible approach for selecting a more comprehensive indicator set by constructing a common correlation matrix to identify indicators that can be used for the assessment of all three scenarios. For the clusters of variables of the common indicator set, the correlations of variable changes remain significant even under different atmospheric carbon or land-use forcing.
However, one should always ask whether the identified clusters and indicators are scientifically meaningful. For the common correlation matrix (as well as the RCP8.5 scenario), the first indicator, “atmospheric CO2” (A_co2), groups together variables describing changes in carbon fluxes, temperatures, and moisture fluxes over the ocean. This is scientifically meaningful, since changes in carbon fluxes will affect the atmospheric carbon content and hence atmospheric temperatures, both over land and ocean. These temperature changes in turn have an effect on the moisture fluxes over the ocean, such as the evaporation over ocean, which is physically driven by temperature changes. These categories are hence physically linked, and it is to be expected that they are correlated irrespective of the forcing scenario chosen.
The second indicator, “precipitation over land” (F_precipL), represents the variability of moisture fluxes on land and the associated cooling effect. The fact that these processes are clustered under an indicator that is distinct from global and oceanic moisture fluxes indicates different underlying processes for these moisture fluxes, namely the influence of biological transpiration. This process is directly affected by the parameter perturbations concerning the sensitivity of transpiration to CO2 (Mengis et al., 2015) and the CO2 fertilization effect (Matthews, 2007). Given the parameter sensitivities of the model considered, the distinction between terrestrial and marine moisture fluxes is scientifically meaningful.
Another identified cluster is “net top-of-atmosphere radiation” (F_netrad) and “ocean surface heat flux” (F_heat), which are directly linked in the model. Furthermore “net surface downward shortwave radiation” (F_dnswr) and “land surface albedo” (A_albsurL) are clustered, since changes in vegetation on land induced by the parameter perturbations influence both the surface albedo on land and the incoming shortwave radiation at the surface.
The “air-to-sea carbon flux” (F_carba2o) and “soil respiration” (L_soilresp) are clustered together for all three scenarios but show a negative correlation of variable changes in the historical scenario and positive correlations of variable changes in the two RCP scenarios, indicating a dependency on the atmospheric carbon concentrations. The predominant parameterization for those correlations of variable changes is one that affects the CO2 fertilization (Fig. S7). Since this is not an intuitive connection, we will briefly discuss this correlation in more detail: the strength of the CO2 fertilization determines the increase in plant net primary production (NPP) to increasing atmospheric CO2 concentrations. For the historical scenario, in the case when the CO2 fertilization parameterization is increased, soil respiration increases due to an increase in vegetation and hence the soil carbon pool. In the same case, the air-to-sea carbon flux slightly decreases due to lower atmospheric carbon concentration in the case of increasing vegetation NPP and consequently land CO2 uptake. Hence, the negative correlation of variables changes between the “air-to-sea carbon flux” (F_carba2o) and “soil respiration” (L_soilresp) for the CO2 fertilization perturbation in the historical scenario (Fig. S7a).
In contrast, in the future, high-CO2 and temperature scenarios both Earth system variables show larger changes with increased CO2 fertilization parameterization. For “soil respiration” (L_soilresp), the underlying process remains the same in this case. However, the terrestrial carbon reservoir reaches a saturation state during the high-emission scenarios. With increasing CO2 fertilization strength the land carbon reservoir reaches this saturation state earlier, causing more carbon to remain in the atmosphere, which following Henry's law results in an overall higher “air-to-sea carbon flux” (F_carba2o) in the simulations with higher CO2 fertilization, since the ocean equilibrates with the atmosphere. This explains the positive correlation of variable changes under the two RCP scenarios.
Two clusters are identified in both future emission scenarios, namely “ocean phytoplankton” (O_phyt), which is clustered with “ocean surface phosphate” (O_po4sur) and “ocean surface nitrate” (O_no3sur), and “ocean oxygen” (O_o2), which is clustered with “ocean surface alkalinity” (O_alksur) (compare Figs. S6 and S7). These two clusters are only identified when atmospheric CO2 concentrations are high but do not hold for the historical scenario, where other relationships seem to be of greater importance. As a result, all of these variables are unclustered for the common indicator selection, causing the number of selected indicators for a common indicator set to increase.
4.1.2 Limitation of the analyses from the example
For our case study, we chose to assess the uncertainty of the biological system towards increasing temperature and CO2, which is reflected in the choice of the considered perturbed parameters. In addition to directly perturbing biological parameterizations, we also perturbed some key physical parameters that indirectly influence the biological systems. All parameter perturbations were chosen because the parameterizations are poorly constrained, and under future high-CO2 and temperature forcing, it will be become increasingly important to take this uncertainty into account. These choices, however, bias the correlation analysis of the model output variables towards their sensitivity to the selected perturbations (for a detailed discussion, see Sect. 3 and Fig. S4 in the Supplement). For a more comprehensive assessment of uncertainties, experiments with different uncertainties in the simulated Earth system, such as cloud parameterizations or the model's climate sensitivity, would need to be considered. Such experiments would accordingly change the patterns of the correlation matrix. Furthermore, to take into account the nonlinearity of the Earth system, as a follow-up study, one could covary the parameters. This would more realistically reflect the inherent process uncertainty within an Earth system model.
It is important to stress the fact that the Earth system variables used in our example are annual global integrals or means between two fixed points in time. While our approach was sufficient to demonstrate the SCoMaE method, it is important to mention that global integrals and means are not always positively correlated to regional changes and, therefore, may misrepresent regional responses. Furthermore, we are not assessing the detailed temporal development of the model variables' response to changes in the climate state. Instead, we investigate changes in the final simulated climate state imposed by parameter perturbations, which are sensitive to CO2 and temperature, under different climate forcing scenarios. This approach was chosen since the UVic ESCM is a model with low internal variability and would, hence, likely overestimate information if we were to evaluate temporal correlations. Investigating the model's sensitivity to the parameter perturbations was therefore deemed a better choice for illustrating the SCoMaE method. Any more thorough climate change assessment using the SCoMaE method would also need to investigate how variable correlations and indicator clusters might change spatially and temporally.
4.2 Discussion of the SCoMaE method
The construction of an individual or a common correlation matrix can be a useful tool for assessing the state of complex systems. Individual correlation matrices allow one to obtain an initial overview of relationships between the different system variables, whereas a common correlation matrix shows how changes in the state of a system, imposed by, e.g., varying forcing scenarios, influence these relationships. The SCoMaE method then allows us to cluster the variables, based on statistical considerations, to obtain a nonredundant indicator set to guide more detailed analysis.
However, in order for this to be useful one must carefully select, what information to include in the correlation matrix, which in turn strongly depends on the given research question. This can be illustrated by the implicit choices made for our example case study, where we regarded correlations of variable changes in globally averaged model output variables given various parameter perturbations. The first choice in this case study was to use global aggregates of the model output. However, if the research focus were set on, e.g., regional phenomena, the correlations for the matrix could also be constructed either between regional aggregates or based on the correlation strength for a given spatial pattern.
The second choice for the case study, was to regard correlations between changes in model output variables based on their reaction to a parameter perturbation under changing climate forcing. Instead of using model output, it is also possible to further process the data and calculate derivatives of the model output variables, such as heat stress or cumulative time series. On another note, using a model with higher internal variability, it would also be possible to regard temporal correlations of Earth system variables over a chosen time period. In contrast to the purely process-based parameter perturbations that we regarded in the case study, this would hold information about the timescales and temporal development of the model output variables, which, in turn, could indicate common underlying processes in the model. Additionally, if the considered time series showed higher internal variability, it might be conceivable to apply a specific temporal filter to the data before calculating the correlation matrix. This could allow the distinction between important processes on different timescales, from daily and seasonal to interannual or decadal.
In the following we want to discuss the contribution of the SCoMaE method to achieve the three characteristics for indicator selection as introduced by Radermacher (2005). Constructing a correlation matrix enables scientists to comprehensively identify correlations in complex systems, such as the Earth system, both simulated and observed. The application of SCoMaE allows one to identify scientifically consistent sets of indicators, which are independent and hence do not provide redundant information, to be used in a science-led assessment. This method represents a bottom–up, natural-science perspective on indicator selection. It thereby tackles one of the three characteristics discussed by Radermacher (2005), namely that of scientific consistency.
In our example the SCoMaE method is based on model data and hence does not account for information about the statistical measurability of the identified indicators. This makes it difficult to directly translate a model-based indicator set to a “real-world” application. This is the case, for example, for the first indicator in the historical scenario: “precipitation over ocean” (F_precipO). The lack of long-term historical precipitation measurements over the ocean (New et al., 2001) would prevent this indicator from being used in a real-world application. It is, however, noteworthy that there is value in the knowledge that this variable could hold information about other Earth system variables, and hence it might be worth improving the observational system.
The third characteristic mentioned by Radermacher (2005) is the political relevance of indicators. Since SCoMaE is a bottom–up, science-led approach for indicator selection, it at first does not take into account political, ethical, and economical considerations. However, these considerations as well as measurability constraints can be included in the analysis. Prescribing a certain indicator, e.g., “surface air temperature” (A_sat) in Sect. 3.5, SCoMaE allows us to include expert judgment and enables us to identify the remaining indicators needed for a fully comprehensive assessment. An iterative learning process for which indicators are societally relevant and scientifically consistent as proposed by Oschlies et al. (2017) and Singh et al. (2015) would hence allow the SCoMaE method to identify scientifically meaningful, measurable, and politically relevant indicators sets.
In this study we introduced a bottom–up, correlation-based approach to systematically identifying indicator sets for the assessment of complex systems. To demonstrate the SCoMaE method, we applied it to correlation matrices constructed with changes in Earth system variables of an intermediate-complexity Earth system model, with which we simulated three forcing scenarios. We were able to identify indicator sets for an assessment of the historical as well as for an intermediate–high and a business-as-usual future emission scenario. The comparison of the three correlation matrices yielded the opportunity to assess changes in correlations between changes in Earth system variables introduced by the imposed forcing. These changes in the correlation patterns also motivated a reevaluation of the selected indicator sets for the different scenarios. We show that it is not sufficient to apply the indicator set identified for the historical scenario to the intermediate–high nor to the business-as-usual future emission scenario. This result points to the fact that the classical procedure of ad hoc indicators, such as surface air temperature, may work well for certain environmental conditions or scenarios but possibly not as well for others. That is, the subjective choice of indicators may lead to unintended preferences in the interpretation of different scenarios. By combining the three scenarios into a common correlation matrix, we could identify correlations between changes in Earth system variables that are robust across the three forcing scenarios. Considering these correlations only enabled us to identify a common indicator set, which was scientifically consistent and would allow us to comparatively assess the three considered scenarios.
This case study is one example out of many possible applications of the correlation matrix and SCoMaE method. The construction of the correlation matrix can be adjusted to the respective research question, which makes the SCoMaE method a generic and flexible tool. An iterative application of the SCoMaE method offers the user the chance to comprehensively assess complex systems such as the Earth system, while including political, ethical and economical considerations, as well as measurability constrains.
The model data used to generate the figures will be made available at http://thredds.geomar.de.
The supplement related to this article is available online at: https://doi.org/10.5194/esd-9-15-2018-supplement.
NM, AO, and DPK conceived of and designed the experiments. DPK and NM implemented and performed the experiments. NM analyzed the data and wrote the manuscript with contributions from DPK and AO.
The authors declare that they have no conflict of interest.
The authors thank Wilfried Rickels, Martin Quaas, and Christian Baatz for
their helpful comments, as well as the participants of the Metrics Workshop
of the SPP 1689 in Hamburg in March 2015 for their thoughts on metrics and
indicators. This work was funded by the DFG Priority Program “Climate
Engineering: Risks, Challenges, Opportunities?” (SPP 1689).
Edited by: Ben Kravitz
Reviewed by: two anonymous referees
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