ICON in Climate Limited-area Mode (ICON release version 2.6.1): a new regional climate model
- 1Deutscher Wetterdienst, Frankfurter Str. 135, 63067 Offenbach am Main, Germany
- 2Helmholtz-Zentrum Geesthacht, Max-Planck-Str. 1, 21502 Geesthacht, Germany
- 3Brandenburg University of Technology, P.O. Box 10 13 44, 03013 Cottbus, Germany
- 4Freie Universität Berlin, Carl-Heinrich-Becker-Weg 6-10, 12165 Berlin, Germany
- 5Deutsches Zentrum für Luft- und Raumfahrt, Institut für Physik der Atmosphäre, Oberpfaffenhofen, Germany
Correspondence: Trang Van Pham (email@example.com)
For the first time, the Limited-Area Mode of the new ICON (Icosahedral Nonhydrostatic) weather and climate model has been used for a continuous long-term regional climate simulation over Europe. Built upon the Limited-Area Mode of ICON (ICON-LAM), ICON-CLM (ICON in Climate Limited-area Mode, hereafter ICON-CLM, available in ICON release version 2.6.1) is an adaptation for climate applications. A first version of ICON-CLM is now available and has already been integrated into a starter package (ICON-CLM_SP_beta1). The starter package provides users with a technical infrastructure that facilitates long-term simulations as well as model evaluation and test routines. ICON-CLM and ICON-CLM_SP were successfully installed and tested on two different computing systems. Tests with different domain decompositions showed bit-identical results, and no systematic outstanding differences were found in the results with different model time steps. ICON-CLM was also able to reproduce the large-scale atmospheric information from the global driving model. Comparison was done between ICON-CLM and the COnsortium for Small-scale MOdeling (COSMO)-CLM (the recommended model configuration by the CLM-Community) performance. For that, an evaluation run of ICON-CLM with ERA-Interim boundary conditions was carried out with the setup similar to the COSMO-CLM recommended optimal setup. ICON-CLM results showed biases in the same range as those of COSMO-CLM for all evaluated surface variables. While this COSMO-CLM simulation was carried out with the latest model version which has been developed and was carefully tuned for climate simulations on the European domain, ICON-CLM was not tuned yet. Nevertheless, ICON-CLM showed a better performance for air temperature and its daily extremes, and slightly better performance for total cloud cover. For precipitation and mean sea level pressure, COSMO-CLM was closer to observations than ICON-CLM. However, as ICON-CLM is still in the early stage of development, there is still much room for improvement.
In 1999, the limited-area weather forecast model LM (Lokalmodell, Doms and Schättler, 1999; later COSMO, Baldauf et al., 2011), which was developed by the Deutscher Wetterdienst (DWD, the German Meteorological Service), became operational together with the “Global-Modell” (GME) global model (Majewski and Ritter, 2002). A few years later, it was renamed into the “COSMO model” in order to reflect that further development has become a joint task of the COnsortium for Small-scale MOdeling (COSMO). In 2002, the Climate Limited-area Modeling Community (CLM-Community) developed the first version of the regional climate model named CLM. In 2007, the developments in COSMO and CLM were recombined and a first unified version of the weather forecast and climate modes, named COSMO-CLM (Rockel et al., 2008), was released.
In 2001, a cooperation between DWD and Max Planck Institute for Meteorology (MPI-M) was initiated, with the aim to develop a new modelling system for weather forecast and climate prediction. The new system was intended to replace the existing system COSMO/GME for operational weather forecast on one side and, on the other side, the global climate and Earth system model, ECHAM6/MPI-ESM (Stevens et al., 2013; Giorgetta et al., 2013). As a result of this initiative, the ICON (Icosahedral Nonhydrostatic) global numerical weather forecast model (Zängl et al., 2015) was developed and replaced GME as the operational model at DWD on 20 January 2015. As a next step, in December 2016, ICON-EU-Nest, the regional ICON on the European domain interactively nested within the global ICON, replaced COSMO-EU (high-resolution COSMO model configuration for Europe) for higher-resolution forecasts on the European domain. In the second half of 2020, the convection-permitting configuration of ICON Limited-Area Mode (LAM) (ICON-D2) became pre-operational. According to the plans, ICON-D2 will replace the high-resolution COSMO-D2 for the German domain in early 2021 and DWD will stop the operational use of the COSMO model after more than 20 years. This implies that the next unification of COSMO and COSMO-CLM (COSMO 6), scheduled for the end of 2020, will be the last one. Afterwards, the support for COSMO and COSMO-CLM will be gradually reduced.
In this work, we prepared state-of-the-art tools for climate applications for the upcoming years. Starting in 2017, DWD and the CLM-Community decided to develop a new regional climate model (ICON-CLM) based on ICON-LAM. The preparation of ICON-CLM was triggered at DWD in the project ProWaS (Projection Service for Waterways and Shipping) – a joint pilot programme of several German federal agencies – to prepare a regular federal forecasting and projection service about the influence of climate change on coastal and waterway traffic.
ICON can be used on a wide range of scales from climate projection, climate prediction, numerical weather prediction (NWP) down to large-eddy simulations (Heinze et al., 2017). For these different scales, there is a number of different modes, as shown in Fig. 1. Generally, there are three different physics packages available: the NWP, the ECHAM physics and the large-eddy simulation physics (LES physics). Within the first physics package, at global scale, ICON-NWP is used for operational weather forecasting at DWD. ICON-EU-Nest is the regional ICON on the European domain nested within the global ICON-NWP. ICON-LAM denotes the Limited-Area Mode of ICON-NWP, which is currently available for the NWP and large-eddy configurations. ICON-LEM (ICON Large Eddy Model) applies the physics package dedicated to large eddy simulations to study processes such as cloud, convection and turbulence on a very-high-resolution grid. Within the ECHAM physics package, the ICON-A global atmospheric model (Giorgetta et al., 2018), originating from the ECHAM6 general circulation model, is used for global climate simulations. This configuration is coupled to the ICON-O global ocean model (Korn, 2017) and the JSBACH land and biosphere model (Brovkin et al., 2013) within the ICON Earth System Model (ICON-ESM). The feature for one- or two-way nested subdomains with grid refinement available in the NWP physics package (ICON-EU-Nest) has recently also been transferred to the ECHAM package by DWD (ICON-EUClim).
ICON-CLM builds upon ICON-LAM and currently contains a set of technical adaptations for climate applications.
The aim of this paper is to introduce the new regional climate mode of ICON (ICON-CLM) along with its starter package (ICON-CLM_SP), a supporting infrastructure needed to perform long-term simulations. Different technical tests and tests on the impact of prescribing upper boundary conditions interpolated from reanalysis data were carried out. A long evaluation simulation driven by ERA-Interim reanalysis (Dee et al., 2011) was conducted over a period of 20 years and the results were compared to the evaluation simulation of the latest COSMO-CLM version recommended by the CLM-Community (called the “recommended version”, CCLM v5.0_clm9). The paper is structured as follows: some related general information on ICON-NWP and ICON-LAM is provided in Sect. 2. The adaptations in model source code and technical infrastructure are described in Sect. 3. Section 4 gives details of the ICON-CLM model configuration and setup for the evaluation run, as well as the evaluation methods we used. Results of the technical tests and the evaluation run in comparison to observational data and the results of the latest COSMO-CLM version are shown in Sect. 5. Conclusions are provided in Sect. 6.
All ICON models in the ICON family (Fig. 1) utilize unstructured triangular grids that originate from a spherical icosahedron with 20 equal-sized triangles. The ICON horizontal grid is denoted as RnBk; this is a triangular grid generated from the original icosahedron by first dividing the edges into n parts, followed by k subsequent edge bisections. The division of the edges into n equal parts gives n2 spherical triangles within the original triangle. In the second step, each triangle is again subdivided into four smaller triangles. The resulting RnBk grid therefore has the total number of triangle cells ncells and the number of edges nedges calculated from the following formulas:
The average area of the triangles is then equal to the Earth's surface divided by the number of triangles ncells. The effective grid is defined as a square which has the same area as the average triangle area, and the effective grid size is defined as
It can be drawn from Eq. (2) that the effective grid size is around 0.658 times the size of the average triangle grid size. Some characteristics of the model grids used and mentioned in this work are listed in Table 1. Figure 2b visualizes the R2B8 grid extracted from the Coordinated Regional Climate Downscaling Experiment – European domain (EURO-CORDEX) (marked in the red box in Fig. 2a).
The vertical layer distribution in the ICON models is a height-based coordinate system following the terrain, with denser layers near the Earth's surface and gradually changing to constant height model levels above a certain height. Two options for the height-based terrain-following vertical coordinate are offered in the ICON models: the terrain-following hybrid Gal-Chen coordinate (Simmons and Burridge, 1981) and the smooth level vertical (SLEVE) coordinate (Schär et al., 2002; Leuenberger et al., 2010). With SLEVE (used in the simulations in this paper), the influence of small-scale terrain features decays quicker with height than the large-scale features in order to obtain smooth vertical coordinate levels at mid and upper levels. The vertical coordinate is a function of model top height, the layer thickness of the lowermost layer, the total number of vertical layers and the stretch factor which controls the distribution of the model levels. Users can define the vertical model levels by setting these controlling parameters via the model namelist.
Outputs in the ICON models can be written out in GRIB or NetCDF format. Options for outputting on the ICON native grid or regular latitude–longitude (lat–long) grid or rotated lat–long grid are available. Outputs can be written with individual or multiple fields in an output file. Users can define how many output steps can be in one output file and the output frequency. It is possible to have outputs with different intervals, for example, hourly precipitation, daily temperature and monthly mean sea level pressure (MSLP), in the same run.
At the lateral boundary of the limited-area domain, a sponge layer is applied, within which the internal flow is gradually relaxed towards the external boundary data. At the outermost area of the limited domain, the “lateral boundary zone” is a stripe fixed with four cell rows. Here, the external boundary data are simply prescribed. Following the outer four cell rows is the “lateral boundary nudging zone”. The width of this nudging zone can be defined in the namelist setting of ICON with the minimum value of eight cell rows to prevent the boundary artefacts. The nudging coefficient gradually reduces from the outer to the inner edge of the “lateral boundary nudging zone”, making the influence of the prescribed external data weaker. The strength of the nudging can be controlled by the maximum relaxation coefficient in the model namelist.
For the upper boundary, ICON-LAM offers an option of prescribing the upper boundary conditions by using the same driving data source as for the lateral boundary conditions (nudging option). Users can define the height of the nudging zone as well as the nudging coefficients for the horizontal wind and the thermodynamic variables via namelist settings. If this vertical nudging option is turned off, a Rayleigh damping is applied to the vertical wind speed within the damping layer in order to prevent unphysical reflection of vertically propagating gravity waves.
As the Limited-Area Mode of ICON, which ICON-CLM builds upon, has originally been developed for NWP applications, several adaptations and technical extensions were necessary to prepare the model for climate applications. Apart from the adjustments in the code, long-term climate simulations require a technical infrastructure for data and job management. Such an infrastructure has also been developed based on the existing infrastructure of COSMO-CLM.
3.1 The ICON-CLM regional climate model
Weather forecasting, which predicts the state of the atmosphere only up to about 2 weeks in advance, often does not involve the development of the ocean state. Hence, the ocean surface condition is often kept constant during the forecasts in weather prediction models or just slightly adjusted with a climatological trend for the forecast period. Thus, in ICON-LAM, there is only option to update the sea surface temperature (SST) and sea-ice cover monthly. For ICON-CLM, we want to have a flexible option to update of SST and sea ice from external data at a user-defined interval. For this purpose, an option for flexible update frequencies of these boundary conditions was implemented in ICON-CLM. Time-dependent SST and sea-ice data can now be read from external data files and are fed to ICON-CLM with shorter intervals than 1 month (e.g. 1-hourly or 6-hourly). The user can select this option of frequent update of SST and sea ice via namelist settings. The external SST and sea-ice data must be prepared and remapped to the ICON grid.
Similarly, the greenhouse gas (GHG) values are usually kept constant in weather forecast models, because the changes during the forecast period are negligible. In climate projections, however, it is necessary to use the time-dependent GHGs as provided by corresponding GHG scenarios. Such an option was already available in ICON but only in combination with the ECHAM physics package. The corresponding read routine was therefore extended so that it works for the NWP physics as well. Some additions to the NWP radiation scheme were made with respect to the GHG vertical profile with a new option to retrieve the profile from external gas data. A file that contains yearly values of CO2, CH4, N2O and chlorofluorocarbons (CFCs) for all years of the experiment needs to be prepared in advance. These features of the time-dependent SST and GHG were largely based on the corresponding implementations in ICON-A (Giorgetta et al., 2018).
In the NWP configuration of ICON-LAM, the number of soil layers is always constant with eight layers. The depths of half soil layers are also fixed at values between 5 mm and 14.5 m. However, for climate simulations in domains other than Europe (e.g. Africa, Asia) or to achieve better simulation of the soil variables for the European domain, it is usually reasonable to adjust these soil parameters. Therefore, an option for a flexible number and depth of the soil layers has been implemented in the ICON-CLM code.
The input/output of ICON-CLM has also been adjusted to have more flexibility. In NWP mode, the precipitation data are accumulated from the start of the forecast till the end without any reset. This is suitable for short weather forecasts, but for long climate simulations, this procedure is inconvenient and could, in the worst case, cause problems due to data imprecision. Furthermore, the maximum and minimum 2 m temperature values are calculated for 6-hourly intervals in NWP applications, while for climate simulations the standard for these output variables is usually 24 h. To control this flexibility extension, new namelist parameters were introduced in ICON-CLM.
At the lateral boundaries, ICON-LAM requires, by default, information on cloud liquid water content and cloud ice water content from the global forcing data. These input fields are usually available if the ICON-CLM lateral boundary conditions are taken from reanalysis data like ERA-Interim. But if global climate projections are used as lateral boundary conditions, these fields are usually not provided. Thus, the model code has been adjusted so that if cloud liquid water content and cloud ice content are not available in the lateral boundary data, these variables are initialized with zero.
Table 2 provides an overview of some differences between COSMO-CLM and ICON-CLM.Doms et al. (2011)Orr et al. (2010)(Tiedtke, 1989)Tiedtke (1989)Tiedtke (1989); Bechtold et al. (2008)Seifert and Beheng (2001)Doms et al. (2011); Seifert and Beheng (2001)Ritter and Geleyn (1992)Mlawer et al. (1997); Barker et al. (2003)Doms et al. (2011)Schrodin and Heise (2001); Schulz et al. (2016)(Gal-Chen and Somerville, 1975)Schär et al. (2002)(Simmons and Burridge, 1981)Schär et al. (2002)Leuenberger et al. (2010)
3.2 The ICON-CLM_SP starter package
In order to facilitate long-term climate simulations, we developed a runtime infrastructure called starter package and a separate evaluation tool. Both are provided along with the ICON-CLM model source code. The ICON-CLM_SP starter package contains a run routine, a climatological test suite, all necessary utilities and configure scripts for different supercomputing environments. At the moment, two system settings for Nec-Aurora (DWD) and Atos/Bull (DKRZ) are supported and tested (note that our ICON-CLM simulations in this paper were done on the DWD Cray XC40; this computer was replaced by the Nec-Aurora afterwards). Settings for other machines could be easily added if necessary.
The run routine in ICON-CLM_SP, called “subchain”, was adapted from the routine of the existing COSMO-CLM package. The “subchain” contains five subroutines for input preparation (prep), converting input data (conv2icon), ICON-CLM job management (icon), archiving (arch) and postprocessing (post) of the model output. Subroutine “prep” copies and checks all the global forcing data as input for “conv2icon”. Then “conv2icon” preprocesses and interpolates the initial data and the lateral, lower and upper boundary data onto the ICON-CLM model grid for the current model simulation. Subroutine “icon” does the job management for ICON-CLM model. After that, all model output data are compressed by “arch” and some post-processing steps like the provision of time series of selected output variables are done in “post”. Usually the simulations in ICON-CLM are done per calendar month with restarts at the end of each month; however, the simulation duration can be easily customized by changing in the subroutine “icon”.
A climatological test suite (CTS) was also created based on the CTS from COSMO-CLM. In the CTS, 5-year test simulations can be done automatically with “subchain”. The users can choose one simulation as a reference. The test simulations then will be compared with the reference simulation with respect to observational data (E-OBS and Climate Research Unit (CRU); see Sect. 4.2 for more details) by an extra subroutine called “eval”. At the end, the results are visualized with standardized plots. This CTS was built for the purpose of testing different versions of model source codes or different setups of the same model version. Hence, it is a very helpful tool for model development and tuning.
Besides the “eval” subroutine in CTS, a separate evaluation tool called “ETOOLS” was also adapted from the COSMO-CLM evaluation tool. This tool provides comparisons of the simulation results with observation datasets and creates standardized plots to visualize the results. In order to facilitate the transition from COSMO-CLM to ICON-CLM for the users, both ICON-CLM_SP and ETOOLS were created such that the “look and feel” as well as the usage of the software packages are as similar as possible to the corresponding packages that exist for the COSMO-CLM model. The output structure of ICON-CLM or post-processed time series from “subchain/post” are also similar to those of COSMO-CLM for the same reason. On this account, users should be able to use all existing scripts and programmes that were developed for COSMO-CLM output also for ICON-CLM data.
4.1 Model configuration and experiment setup
All of the ICON-CLM tests described afterwards and the evaluation run were performed at R2B8 resolution (approximately 10 km) on a domain (Fig. 2a) completely covering the EURO-CORDEX domain (Giorgi et al., 2009). The model atmosphere is divided into 70 vertical layers and the model top is at a height of 30 km or 10 hPa. The soil in ICON-CLM contains eight layers down to a depth of 14.5 m. ICON-CLM was driven at the lateral and lower boundaries by ERA-Interim at 6-hourly intervals. The model atmosphere was initialized with ERA-Interim data. The soil temperature and soil moisture were taken from a previous simulation which is long enough to ensure that the spin-up of the soil has been completed. The monthly Tegen aerosol climatology (Tegen et al., 1997) and the ozone climatology from Global Earth-system Monitoring using Satellite and in situ data (GEMS) were used in our simulations. For the upper boundary, as described in Sect. 2, there are two options: (1) using the driving data and nudging gradually in the relaxation zone; (2) damping the vertical wind beneath the upper boundary. To assess the impact of these two options, two 10-year simulations (1979–1988) were done with the same setup, with and without global data nudging. Analysis from these 10-year runs resulted in very minor differences on surface variables and none of the options showed any advantage over the other. For the evaluation run, we chose the option with nudging data at the upper boundary with ERA-Interim data, as later we wanted to compare the results with those from a COSMO-CLM run using a similar nudging option. The nudging zone started from the height of 12 km to the model top of atmosphere (30 km). Variables which are nudged within this layer are the horizontal wind and the thermodynamic variables (air pressure and temperature) with nudging coefficients of 0.04 and 0.075, respectively.
In order to find a suitable model configuration for ICON-CLM at R2B8 resolution, an optimized namelist setup was used, namely the setup from ICON-NWP for R3B7 with nested domain on R3B8 grid (approximately 13 and 6.5 km, respectively). The tuning parameters were taken over from the global settings. In this setting, the Tiedtke–Bechtold (Bechtold et al., 2008) convection parameterization scheme and the Rapid Radiation Transfer Model (RRTM) radiation scheme (Mlawer et al., 1997) were used. These setups were checked to make sure that they were appropriate for climate applications and were used in all simulations.
Former simulations (not published) with COSMO-CLM showed that in some cases the model results depended on the chosen model time steps. There was one particular time step that led to larger biases in precipitation and surface pressure, especially over the Alps and the southwestern area of the EURO-CORDEX domain. This issue has been analysed by the CLM-Community but is still not fully understood yet. To ensure that such a dependency of the results on the model time step is not present in ICON-CLM, different fast physics/advection time step (hereafter time step) choices were tested. At R2B8 (approximately 10 km) resolution, the time step should not exceed 120 s for stability reasons. With the common model and experiment setups described above, we carried out multiple 1-year simulations for the year 1979 with time steps of 60, 80, 90, 100 and 120 s. Figure 3 shows the biases compared to reference data of 2 m temperature, total precipitation, MSLP and total cloud cover. The biases were averaged for each month and for the Alpine region (subregion denoted AL in Fig. 2c). Colours show the different time step experiments. The biases for all variables from any particular time step experiment were small and did not stand out from the rest. Similar results were found for all other subregions and therefore are not shown here. The annual and seasonal biases of these multiple 1-year simulations were also very similar to all time steps (not shown here).
Because there is no big difference in the model results depending on the choice of time step, for experiments at the R2B8 spatial resolution, we chose the time step of 90 s due to the computational efficiency and stability, the time step of COSMO-CLM at similar horizontal resolution is 100 s. An evaluation run was carried out for the EURO-CORDEX domain at the R2B8 resolution. The simulation period is 1979 to 2000. The model and experiment setups were the common setups as described above, this evaluation run is later referred to as ICLM-REF.
The results of ICLM-REF were compared to the reference experiment of the recent recommended version of COSMO-CLM (v5.0_clm9). This COSMO-CLM simulation is later referred to as CCLM-REF. This COSMO-CLM setup showed the best performance for the EURO-CORDEX domain in an intercomparison with a large number of setups which was performed within the COPAT project (COordinated Parameter Tuning, a project providing a thorough evaluation of a large number of COSMO-CLM configurations to come up with a recommended version) in the CLM-Community. The simulation period is 1979 to 2000; the model resolution is 0.165∘, also about 10 km like in ICLM-REF. The initial, lower and lateral boundary data are taken from ERA-Interim. A sponge layer with Rayleigh damping in the upper levels of COSMO-CLM domain was used. The damping was done against the external boundary values, similarly to the nudging at the model top in ICLM-REF simulation, and thus the results from both experiments are comparable.
4.2 Evaluation methods
For model assessment and evaluation, output fields from six variables were analysed, namely 2 m temperature, daily maximum and minimum values of 2 m temperature, MSLP, total precipitation and total cloud cover. Monthly average values of these variables were calculated and used for further analysis. For total precipitation, the monthly accumulated amounts were calculated. Parts of the evaluation were carried out based on seasonal averages. The following definitions and abbreviations of the seasons are used in this paper: winter – December, January, February (DJF); spring – March, April, May (MAM); summer – June, July, August (JJA); and autumn – September, October, November (SON). Results were averaged for eight subregions as already used in the Prediction of Regional scenarios and Uncertainties for Defining EuropeaN Climate change risks and Effects (PRUDENCE) projects (described by Christensen and Christensen, 2007). These subregions are the British Isles (BI), Iberian Peninsula (IP), France (FR), Mid-Europe (ME), Scandinavia (SC), Alps (AL), Mediterranean (MD) and Eastern Europe (EA) (shown in Fig. 2c).
For the evaluation of mean values of 2 m temperature, daily maximum and minimum 2 m temperature, MSLP and total precipitation, the E-OBS dataset (Haylock et al., 2008; Van den Besselaar et al., 2011) was used as reference data. E-OBS is a 0.25∘ gridded daily dataset covering all of Europe. The data are available over land from quite recently back to 1950. In order to compare 2 m temperature data from different datasets (ICLM-REF, CCLM-REF and E-OBS), a height correction was performed. The model temperature values at E-OBS 2 m height were calculated based on the differences between model and E-OBS surface elevation and the moist adiabatic lapse rate (0.0065 K m−1). The reference cloud data, which were used for assessment of the model cloud cover, are CRU time series (TS) data (Harris et al., 2014). This is a monthly gridded dataset at 0.5∘ resolution, available globally over land area. The dataset covers the period from 1901 to 2013.
For all ICON-CLM simulations in this paper, the outputs were written in NetCDF format and on the rotated lat–long grid as in CCLM-REF. Because this rotated lat–long grid is finer than E-OBS and CRU grids, these data were remapped to the regular lat–long grids with the same spatial resolution as the observational data for the purpose of comparison. The E-OBS and CRU datasets contain data only over land; therefore, the evaluation in this paper (e.g. areal averaged fields) were done using only land points.
The evaluation within COPAT for 2 m temperature, MSLP and cloud cover was done using E-OBS version 10.0 and CRU version 3.22 as reference data. Therefore, in order to compare our evaluation to the one from COPAT, we also used the same versions of the datasets. The comparison period is 20 years from 1981 to 2000, the same as the evaluation period in COPAT. The reference total precipitation data were taken from E-OBS version 12.0 because this dataset (among versions from 10.0 to 17.0) shows the fewest missing data for precipitation over the area of Poland.
Some important climate indices (listed in Table 3) were calculated from ICLM-REF, CCLM-REF and E-OBS 2 m temperature and total precipitation data and averaged over the period 1981–2000. The number of days that fulfils the definition (in Table 3) was counted for each horizontal grid cell, then averaged over a subregion.
Root-mean-square error (RMSE) was calculated from the model and observed monthly values (monthly aggregated values for precipitation and monthly mean values for other variables):
where Si and Oi are the model (ICLM-REF or CCLM-REF) and reference data (E-OBS or CRU TS) monthly values, respectively, averaged over the subregions considered at the ith month; N is the total number of months in the evaluation period (1981–2000).
To compare the spatial variability of the data, spatial standard deviation (SD) was also calculated from time-averaged fields of model and observed data. The SD ratio () was calculated for the ease of comparing the spatial variation of the two model data with respect to the observation. The model with SD ratio closer to 1 better represents the spatial variation of the observation data.
The results of air temperature from ICLM-REF were also compared to those of other regional climate models (RCMs) within the EURO-CORDEX experiments. A thorough evaluation of several EURO-CORDEX ensembles is presented in Kotlarski et al. (2014). One ensemble, called EUR-11, has quite a similar setup to our ICLM-REF setup. The horizontal resolution of the RCMs in this EUR-11 ensemble is about 12 km; these simulations were also driven by ERA-Interim. The simulation period, however, differs from ours: 1989–2009 instead of 1981–2000. Nevertheless, this comparison for sure gives us some knowledge about ICON-CLM performance relatively to other state-of-the-art RCMs. In Figs. 5 and B1 in Kotlarski et al. (2014), some similar analysis to ours were done for nine different RCMs, seasonal means of temperature bias are shown for eight PRUDENCE subregions. These biases were also calculated against E-OBS data like in our evaluation, though an older version of E-OBS data was used in their paper. These figures were used to compare to our figures from ICLM-REF.
5.1 Technical tests
After the technical adaptation in the ICON model source code to enable long-term climate simulations, a number of technical tests was performed. First, the influence of different domain decompositions for parallelization on the simulation results was tested on the Cray XC40 supercomputer at DWD. The domain of ICON models is split by a built-in geometric subdivision according to the number of processors used for calculation. Tests with ICON-CLM were done using 120, 240, 480 and 960 computer processors; each test simulated the year 1979. As these tests are 1-year long each, they contain multiple monthly restarts of the model. The model outputs were checked for all climate variables evaluated in this paper. Results were binary identical, independent of the numbers of processors used for the simulating. ICON-CLM showed the ability to produce the same results and to restart properly with a variety of domain decompositions.
Repeating tests starting from the same restart state were also carried out. ICON-CLM was restarted at the time point on 1 January 1980 at 00:00 UTC multiple times from the same restart file on the Cray XC40. Each simulation was carried out for 1 month from 1 to 31 January 1980. Model outputs were checked for all model calculation steps and for all climate variables evaluated in this paper. In addition, the restart files created at the end of each test for the simulation time on 1 February 1980 at 00:00 UTC were also compared. The results from these repeating tests showed binary identical values. Two additional restart tests were also done. In the first test, ICON-CLM was run for 2 months from 1 January to 29 February 1980 without restarting in between. And in the second test, ICON-CLM also simulated these 2 months but was restarted on 1 February 1980 at 00:00 UTC. The model outputs were compared, with a focus on the period after the restart of the second test. Results showed that restarting did not introduce any difference in model diagnostics.
Short tests up to few months were also done on a different computing system, the Atos/Bull at the German Climate Computing Centre (DKRZ). ICON-CLM showed the ability to run stably on at least two machines. Performance tests were done for ICON-CLM and COSMO-CLM on the Atos/Bull. The two models were run in 1-month simulations on the European domain. The horizontal resolution is roughly 50 km; the same number of computer processors was used. ICON-CLM was about 15 % faster than COSMO-CLM in these tests.
5.2 Evaluation and comparison with COSMO-CLM
Initially, a longer simulation with ICON-CLM (30 years) was planned and carried out. But since the data from CCLM-REF are only available to us in the period 1981–2000, only data in this period were taken for evaluation.
5.2.1 Air temperature
The 2 m temperature bias of ICLM-REF and CCLM-REF was mostly within −1.5 to 1.5 K relative to E-OBS data. Figure 4 shows the mean annual biases against E-OBS data over the 20-year period from 1981 to 2000 for ICLM-REF and CCLM-REF data for the entire domain. Both experiments had dominant negative bias over Eastern Europe, with ICLM-REF to a lesser extent. ICLM-REF had a warm bias in most parts of Sweden and southern Russia, while CCLM-REF showed a cold bias in these regions. The Balkan region is well known for large air temperature biases in COSMO-CLM simulations (Anders and Rockel, 2009; Pham et al., 2014; Trusilova et al., 2014), which also occurred in ICLM-REF with values up to 1.5 K.
The seasonal temperature bias in Fig. 5 shows that the median of the bias in the subregions ranged from −0.58 to 0.81 K for ICLM-REF and −1.13 to 1.20 K for CCLM-REF. While in many of the subregions and seasons a relatively small bias was found for ICLM-REF (bias median in the order of 0.01 K), CCLM-REF had usually larger biases. Both models had smaller biases in winter and autumn and larger biases in spring and summer. Besides some subregions like the British Isles, Mid-Europe, France, Iberian Peninsula where small biases were found (especially from ICLM-REF), the Scandinavia, Alps, Mediterranean and Eastern Europe subregions showed larger biases. The latter subregions also showed larger variability of biases in space, with the bias ranges from −3.7 to 3.4 K. CCLM-REF had almost always more variability in temperature bias than ICLM-REF. The differences in spatial variability in CCLM-REF were exceptionally strong in Scandinavia in winter and summer.
Compared with the nine RCMs in EURO-CORDEX ensemble EUR-11 (Kotlarski et al., 2014), ICLM-REF showed a similar magnitude of biases for all four seasons. Our ICLM-REF results in Fig. 5 were placed in comparison to Figs. 5 and B1 in Kotlarski et al. (2014). ICLM-REF and other EURO-CORDEX experiments tended to have negative biases for air temperature in winter. In spring, the opposite was observed; ICLM-REF gave a positive bias for most of the subregions, while EUR-11 continued to have negative biases. In all seasons, ICLM-REF biases stayed well fit within the spread of the EUR-11 ensemble and had smaller biases compared with some other RCMs. In winter, for example, it can be seen on the spread of the solid circles (representing the EUR-11 ensemble) in Figs. 5 and B1 in Kotlarski et al. (2014) that the temperature biases of EUR-11 ensemble were up to −4 and −3 K for the Alps and Mediterranean subregions, respectively, and for other subregions up to around −2 K. Meanwhile, ICLM-REF had mean biases quite close to 0 for most of the subregions (Fig. 5, DJF).
For daily max/min temperature bias, CCLM-REF and ICLM-REF showed opposite results. CCLM-REF tended to underestimate the maximum 2 m temperature, while ICLM-REF overestimated the values. This can be most clearly seen in winter and autumn (Fig. 6), where the medians of almost all ICLM-REF biases were positive and those of most CCLM-REF biases were negative. ICLM-REF clearly had smaller median biases ranging from −0.02 to 2.34 K, while the range in CCLM-REF was −2.5 to 1.2 K. In summer, the bias was larger for both models. CCLM-REF had larger spatial differences among the subregions than ICLM-REF. Similarly, the bias of the minimum 2 m temperature of ICLM-REF was reduced compared to CCLM-REF (−1.2 to 0.5 K compared to −0.6 and 1.8 K, Fig. 7). ICLM-REF slightly underestimated the daily minimum 2 m temperature, while CCLM-REF overestimated it. Consequently, the daily temperature range was overestimated by ICLM-REF and underestimated by CCLM-REF. However, the representation of the daily temperature range is, in general, in ICLM-REF closer to the observed values than in CCLM-REF. The overestimation of the diurnal range of temperature near the surface in ICLM-REF was probably caused by a positive radiation bias, which is known in ICON. This positive bias is especially large when the RRTM radiation scheme (Mlawer et al., 1997; Barker et al., 2003) is used, which was the case in ICLM-REF (see Table 2). Recently, another radiation scheme, named ecRad (Rieger et al., 2019), is added into ICON. The positive bias for radiation is strongly reduced with the use of this radiation scheme.
ICLM-REF had also a smaller RMSE than CCLM-REF for 2 m temperature over most subregions, with one exception in the Iberian Peninsula subregion (Table 4). RMSEs of ICLM-REF did not exceed 0.87 K, whereas CCLM-REF had RMSE up to 1.03 K. Looking at the SD ratio, ICLM-REF had stronger spatial variation than E-OBS in three out of eight subregions and weaker variation in four out of eight. In some subregions, the SD ratio was equal or very close to 1 (France, Iberian Peninsula, Mediterranean). Compared with CCLM-REF, ICLM-REF showed better SD ratios in six subregions.
Similar results were found for minimum 2 m temperature, with RMSE from ICLM-REF between 0.36 and 0.85 K. All ICLM-REF RMSEs were smaller compared to those from CCLM-REF, especially for the Mediterranean and British Isles subregions, ICLM-REF errors were less than half (Table 5). ICLM-REF's SD ratio was closer to 1 for all subregions in comparison with CCLM-REF. Both models did not simulate the minimum 2 m temperature spatial variation as well in mountainous areas (Scandinavia and Alps) as for flatter areas but did not show a tendency towards a specific type of orography.
Regarding RMSEs of maximum 2 m temperature (Table 6), ICLM-REF showed larger biases compared to the biases of min/mean 2 m temperature with a maximum bias of 1.54 K in the Mediterranean subregion. In four out of eight subregions, ICLM-REF had lower errors, and five subregions showed better spatial variation. Overall, ICLM-REF simulated average and daily max/min values of 2 m air temperature better than CCLM-REF.
The improved representation of daily max/min 2 m temperature in ICLM-REF resulted in a reduced bias for climate indices which are determined by air temperature. Among those indices, CCLM-REF overestimated the annual numbers of ice days and tropical nights averaged over the evaluation period (1981–2000), as can be seen in Fig. 11. The largest tropical night overestimation was found for the Eastern Europe subregion with 5.2 nights per year by CCLM-REF, 6.5 times more than that of E-OBS (0.8 nights per year), while the ICLM-REF result was much closer to the observations with only 1.15 nights per year. Besides that, ICLM-REF tropical night indices were very close to the observed numbers for the France, Alps and Mediterranean subregions, while the numbers in CCLM-REF clearly stand out against the observations. The results for the annual ice day index were similar; CCLM-REF overestimated the number of ice days for all subregions. ICLM-REF, on the other hand, slightly underestimated the annual numbers of ice days but was in all subregions much closer to the number derived from E-OBS than CCLM-REF. Generally, ICLM-REF showed an underestimation of the annual frost days compared to observations over Europe, except for the Scandinavia subregion. Compared to CCLM-REF, however, the underestimation was reduced in ICLM-REF. The biggest improvement was simulated in the Alps subregion.
The number of annual summer days was overestimated by ICLM-REF for six of the eight subregions, while CCLM-REF mostly underestimated the amount of summer days. The strongest overestimation of the summer day index compared to CCLM-REF and E-OBS was seen in the Mediterranean subregion. For three out of eight subregions and on average over all of Europe, ICLM-REF simulated summer day indices more in agreement with observations compared to CCLM-REF. On average, for all of Europe, ICLM-REF resulted in 53.25 summer days per year; the numbers from E-OBS and CCLM-REF are 56.4 and 43.7 summer days, respectively.
The mean annual precipitation bias ranged mostly from −50 to 50 mm per month in both models (Fig. 4). Overall, both models simulated more precipitation than E-OBS data. However, one should keep in mind that E-OBS precipitation data tend to suffer from gauge undercatch and evaporation leading to too-low values (Gampe and Ludwig, 2017; Hofstra et al., 2009). That might be the reason why both ICLM-REF and CCLM-REF overestimated precipitation in large parts of the domain. CCLM-REF tended to produce too little precipitation compared to E-OBS along the Atlantic coast, while ICLM-REF agreed better with observations in this area. In the western part of Germany, for example, ICLM-REF had only a slight bias of 5 mm per month compared with the reference data. CCLM-REF, on the other hand, produced negative biases up to −20 mm per month in this area. However, over the eastern part of Germany, ICLM-REF had larger biases up to more than 10 mm per month. In all other regions, the annual spatial distribution of precipitation biases was quite similar in both models.
Looking at the spatial variability of the seasonal biases among the subregions in Fig. 8, we see that although for some subregions in certain seasons, the bias medians were close to zero, the ranges of biases were large. This is expected because precipitation is a highly inhomogeneous variable. Summer and autumn tended to have small median bias in ICLM-REF and CCLM-REF. Among the four seasons, summer had the smallest variation, probably due to the low precipitation amount. For winter, summer and autumn, it is not clear which model performed better. For spring, the median and the range of the bias were in better agreement with observations in CCLM-REF compared to ICLM-REF for most of the subregions.
RMSE for precipitation from ICLM-REF ranged from 10.48 to 30.52 mm (Table 7). The largest error appeared over the Alps subregion, probably due to the complicated terrain and the dependency of precipitation on orography. RMSEs of CCLM-REF were smaller than those of ICLM-REF for most of the subregions, except for the Iberian Peninsula and Scandinavia subregions. ICLM-REF simulated larger variation of precipitation in space compared to E-OBS data, with most SD ratios larger than 1, except for the British Isles with 0.8. The spatial variability of precipitation in CCLM-REF was closer to observations in six out of eight subregions indicated by an SD closer to 1.
ICLM-REF tended to have more precipitation days than CCLM-REF, with the annual wet day index higher for most of the subregions and only one exception for the Scandinavia subregion (Fig. 11). In six subregions, ICLM-REF was more in line with observations than CCLM-REF. ICLM-REF also produced more days with heavy and very heavy precipitation on yearly average than CCLM-REF. For most of the subregions, both models overestimated heavy and very heavy precipitation indices, but CCLM-REF was often closer to E-OBS. From our results, CCLM-REF performed better for precipitation and precipitation-related climate indices. ICLM-REF had in part improvement in certain area of the model domain as well as for a certain season and climate index.
5.2.3 Mean sea level pressure
The biases of MSLP of the two models showed opposite signs. ICLM-REF had positive biases, while the biases in CCLM-REF were mostly negative, as revealed in Fig. 4. ICLM-REF had biases up to 6 hPa, while CCLM-REF had up to −4 hPa. The performance of CCLM-REF was better, especially over Scandinavia and the Iberian Peninsula. The opposite signs of the bias in the two model experiments can also be seen very clearly in Fig. 9. Spring and autumn showed less spatial variability of MSLP values in both models. The representation of MSLP was better in CCLM-REF in winter and autumn than in ICLM-REF with a smaller median bias and smaller bias ranges.
The RMSEs and SD ratios for MSLP are shown in Table 8. ICLM-REF had better RMSE than CCLM-REF in half of the subregions. However, ICLM-REF had some large errors over the Iberian Peninsula and France subregions with RMSEs of 1.90 and 1.71 hPa, respectively. Regarding spatial variation, ICLM-REF gave a better SD ratio than CCLM-REF in most of the subregions. Both models resulted in the largest difference in SD with respect to E-OBS data over the Alps subregion with the ratio of 1.76 for ICLM-REF and 2.09 for CCLM-REF.
Additionally, we evaluated the representation of the large-scale MSLP in ICON-CLM by looking at its spatial MSLP pattern. The driving ERA-Interim data were used for reference, and the ICLM-REF result was also compared to CCLM-REF. The mean spatial fields of MSLP from the three datasets were calculated for the evaluation period (1981–2000). All data were regridded to ERA-Interim grid to ensure a fair comparison and are shown in Fig. 12; the illustration areas are different among the datasets due to the different model domains. As can be seen, ICLM-REF could be able to reproduce the large-scale pattern of MSLP from the forcing data. The pressure structure looks quite similar between ICLM-REF and ERA-Interim, with the low- and high-pressure systems located in the right areas. Because of the small domain of ICLM-REF compared with ERA-Interim, it is hard to view the whole high-pressure system located west of Portugal. But from what we can see, the highest pressure was a bit closer to the coastline in ICLM-REF than in ERA-Interim. This unfortunately was out of CCLM-REF domain. ICLM-REF underestimated the MSLP near Iceland by several hectopascals. CCLM-REF reproduced the MSLP better than ICLM-REF in this area with the magnitude and pattern very similar to those of ERA-Interim.
5.2.4 Cloud cover
The representation of annual mean cloud cover in ICLM-REF looks much better than in CCLM-REF in Fig. 4. CCLM-REF produced too much cloud over Scandinavia and over the eastern part of the domain (up to 0.2, or in percentage 20 %, more cloud cover than CRU TS data). ICLM-REF, on the other hand, had biases of only up to ±10 %. For most regions, the bias was in the range of ±5 %. The overestimation of cloud cover in the Scandinavia and Eastern Europe subregions might be the reason for the cold bias of CCLM-REF in these regions (see Fig. 4).
For seasonal mean, as shown in Fig. 10, however, CCLM-REF showed a smaller negative bias during winter in all subregions (except Scandinavia), and its performance in autumn was comparable to ICLM-REF. ICON-CLM simulated cloud cover noticeably better than COSMO-CLM over the Scandinavia subregion.
The RMSEs of cloud cover did not show much difference between the two simulations, as presented in Table 9. The same conclusion can be drawn for SD ratios; numbers were somewhat similar from both ICLM-REF and CCLM-REF.
5.3 Large-scale information reproduced by ICON-CLM
As the limited-area models are only forced by the global data at their boundaries, inside the limited domain, the regional climate models can more or less freely develop their own circulation. One of the major concerns in regional climate modelling is to what extent the regional climate models modify the large-scale information from the global data (Sanchez-Gomez et al., 2009).
We want to test if ICON-CLM can be able to reproduce the large-scale atmospheric condition from the ERA-Interim forcing data. The geopotential at 500 hPa data from ICLM-REF and ERA-Interim were averaged at different temporal scales: 6-hourly, daily, monthly, seasonal and yearly. Due to the different grids and ERA-Interim lower resolution, ICLM-REF data were remapped to ERA-Interim grid. The spatial correlation coefficient was calculated for each time slot within the evaluation period (1981–2000).
Time series of the correlation coefficient for the different temporal scales are shown in Fig. 13. For all of the timescales we considered, results showed a higher correlation for longer timescales; the correlation is lowest for 6-hourly data and strongest for yearly data. For the 6-hourly and daily means, the mean correlation coefficient over the whole time period (1981–2000) was high: 0.925 and 0.928, respectively. But the correlation for some time slots dropped below 0.8, causing the minimum values of correlation coefficient only over 0.5. ICON-CLM showed correlation coefficients above 0.85 for longer timescales from monthly to yearly scales. With this result, we can conclude that ICON-CLM reproduced well the large scale of the driving data for timescales from monthly to yearly and partially for timescales from 6-hourly to daily.
The new ICON-CLM regional climate model has been derived from the ICON-LAM weather forecast model along with the necessary technical infrastructure and evaluation tools, allowing users to carry out and evaluate long-term regional climate simulations. An evaluation run from the very first version of ICON-CLM showed very promising results. The ICON-CLM results were proven to be independent of the domain decomposition, and restarting with the same configuration gave binary identical results. ICON-CLM did not show any systematic dependency of the results on integration time steps which was found in COSMO-CLM. All tested time steps showed similar results with no bias outliers for any of the chosen values. These time step tests were done with R2B8 model horizontal resolution (about 10 km) over the EURO-CORDEX domain. When choosing another model grid spacing or simulating another domain, tests might be required to affirm these results.
The vertical nudging of the global forcing data at the upper model boundary did not show any notable impact on the climatology of surface variables. This is probably due to the fact that in our settings of ICON-CLM, the top of the atmosphere was at 30 km height. When choosing a lower model top, one might see larger effects of the vertical nudging. Furthermore, in this study, we focused on the near-surface climate and therefore did not look at the upper air layers where larger differences between nudging and no nudging can be found.
Results from the evaluation run showed that ICON-CLM was able to reproduce the large-scale atmospheric circulation from the driving model and the most important climate variables. In comparison with reference data, ICLM-REF biases are of similar magnitude, for certain areas or certain variables, even slightly smaller than CCLM-REF biases. Improvements were visible in ICLM-REF for air temperature and hence temperature-related climate indices. The reason might be that ICLM-REF showed a lower overestimation of cloud coverage over the northern and eastern parts of the domain compared to CCLM-REF. For precipitation and MSLP, the results from CCLM-REF were in better agreement with E-OBS data.
It should be taken into account that ICON-CLM is still in the early stage of development in climate mode, while COSMO-CLM has been developed and applied for NWP and climate applications for more than 20 years and was well tuned with a large number of tested namelist combinations in the COPAT project. Therefore, ICON-CLM has still great potential to improve its model setup, and with growing experience we expect that ICON-CLM results will improve further in the upcoming years.
Comparison for air temperature between ICLM-REF and the EURO-CORDEX ensemble showed that ICLM-REF biases landed in the upper part of the ensemble bias spreads. A broader intercomparison with EURO-CORDEX ensemble is recommended once an optimum setup for ICON-CLM is established.
As written above, only short tests were done on a different computing system other than the Cray XC40 at DWD. More technical tests, therefore, should be done on the Atos/Bull at DKRZ. Also a comparison of the results from different machines will show how ICON-CLM is dependent on the computer systems.
The next step in the ICON-CLM preparation will be a thorough model tuning by testing the sensitivity of the model to a variety of namelist parameters and different combinations of namelist settings in order to find an optimal configuration. Climate simulations on different domains, e.g. CORDEX Africa, will be done to evaluate the ability of ICON-CLM to simulate different climates. So far, only reanalysis-driven simulations have been performed with ICON-CLM, but historical simulations driven by the results of global climate simulations will also be done to test the model performance for this experiment type. Based on a well-evaluated model configuration, regional climate projections will be carried out in order to address the impact of climate change at regional scale. Thus, climate projections, e.g. in the framework of CORDEX, will also be provided with ICON-CLM in the future. We plan to further develop ICON with the aim of unifying the different physics packages currently existing for numerical weather prediction and the climate mode in order to pursue a “seamless prediction” system with one forecasting system which can produce forecasts and projections for all timescales from weather prediction to seasonal and decadal predictions and climate projections.
The ICON model is distributed to institutions under an institutional license issued by DWD. In the case of the institutional license, two copies of the institutional license need to be signed and returned to the DWD. ICON release version 2.6.1 can be then downloaded at https://data.dwd.de (last access: 10 February 2021).
To individuals, the ICON model is distributed under a personal non-commercial research license distributed by MPI-M. Every person receiving a copy of the ICON framework code accepts the ICON personal non-commercial research license by doing so. Or, as the license states, any use of the ICON software is conditional upon and therefore leads to an implied acceptance of the terms of the Software License Agreement. To receive an individually licensed copy, please follow the instructions provided at https://code.mpimet.mpg.de/projects/iconpublic/wiki/Instructions_to_obtain_the_ICON_model_code_with_a_personal_non-commercial_research_license (last access: 10 February 2021). ICON release version 2.6.1 model code with a personal non-commercial research license can be obtained at https://code.mpimet.mpg.de/projects/icon-downloads/files (last access: 10 February 2021).
The starter package ICON-CLM_SP_beta1 can be downloaded from https://doi.org/10.5281/zenodo.3896136 (Pham and Rockel, 2020). The starter package will be shipped with a recommended configuration for EURO-CORDEX domain at R2B8 resolution and will be available for all CLM-Community members.
The forcing data that were used for our simulations are the ERA-Interim data (Dee et al., 2011). Model evaluation was done against E-OBS version 10.0 and 12.0 (Haylock et al., 2008; Van den Besselaar et al., 2011) and CRU TS version 3.22 datasets (Harris et al., 2014).
TVP implemented the adaptations in the model code and ICON-CLM starter package, carried out the experiments and prepared the manuscripts with contributions from all co-authors. CS contributed in the organization and supervision of the work. IK and MM are the source code administrators of ICON-CLM. BR contributed to the ICON-CLM starter package. KK, BR and BF defined the research goals, aims and methodology. DR and GZ contributed in the development of ICON-NWP, the foundation for ICON-CLM.
The authors declare that they have no conflict of interest.
The authors thank all ICON development teams at DWD and MPI-M for providing us with the ICON model code, which was a great basis for our development. The authors thank the colleagues who provided the COSMO-CLM evaluation from the COPAT project.
We acknowledge the E-OBS dataset from the EU-FP6 project ENSEMBLES (http://ensembles-eu.metoffice.com, last access: 10 February 2021) and the data providers in the ECA&D project (http://www.ecad.eu, last access: 10 February 2021).
This research was supported by project ProWas (Projection Service for Waterways and Shipping), Deutscher Wetterdienst.
This paper was edited by Paul Ullrich and reviewed by Sven Kotlarski and one anonymous referee.
Anders, I. and Rockel, B.: The influence of prescribed soil type distribution on the representation of present climate in a regional climate model, Clim. Dynam., 33, 177–186, 2009. a
Baldauf, M., Seifert, A., Förstner, J., Majewski, D., Raschendorfer, M., and Reinhardt, T.: Operational convective-scale numerical weather prediction with the COSMO model: description and sensitivities, Mon. Weather Rev., 139, 3887–3905, 2011. a
Barker, H. W., Stephens, G., Partain, P., Bergman, J., Bonnel, B., Campana, K., Clothiaux, E., Clough, S., Cusack, S., Delamere, J., Edwards, J., Evans, K. F., Fouquart, Y., Freidenreich, S., Galin, V., Hou, Y., Kato, S., Li, J., Mlawer, E., Morcrette, J.-J., O'Hirok, W., Räisänen, P., Ramaswamy, V., Ritter, B., Rozanov, E., Schlesinger, M., Shibata, K., Sporyshev, P., Sun, Z., Wendisch, M., Wood, N., and Yang, F.: Assessing 1D atmospheric solar radiative transfer models: Interpretation and handling of unresolved clouds, J. Climate, 16, 2676–2699, 2003. a, b
Bechtold, P., Köhler, M., Jung, T., Doblas-Reyes, F., Leutbecher, M., Rodwell, M. J., Vitart, F., and Balsamo, G.: Advances in simulating atmospheric variability with the ECMWF model: From synoptic to decadal time-scales, Q. J. Roy. Meteor. Soc., 134, 1337–1351, 2008. a, b
Brovkin, V., Boysen, L., Raddatz, T., Gayler, V., Loew, A., and Claussen, M.: Evaluation of vegetation cover and land-surface albedo in MPI-ESM CMIP5 simulations, J. Adv. Model. Earth Sy., 5, 48–57, 2013. a
Christensen, J. H. and Christensen, O. B.: A summary of the PRUDENCE model projections of changes in European climate by the end of this century, Climatic Change, 81, 7–30, 2007. a
Dee, D. P., Uppala, S. M., Simmons, A. J., Berrisford, P., Poli, P., Kobayashi, S., Andrae, U., Balmaseda, M., Balsamo, G., Bauer, P., Bechtold, P., Beljaars, A. C. M., van de Berg, L., Bidlot, J., Bormann, N., Delsol, C., Dragani, R., Fuentes, M., Geer, A. J., Haimberger, L., Healy, S. B., Hersbach, H., Hólm, E. V., Isaksen, L., Kållberg, P., Köhler, M., Matricardi, M., McNally, A. P., Monge‐Sanz, B. M., Morcrette, J.‐J., Park, B.‐K., Peubey, C., de Rosnay, P., Tavolato, C., Thépaut, J.‐N., and Vitart, F. : The ERA-Interim reanalysis: Configuration and performance of the data assimilation system, Q. J. Roy. Meteor. Soc., 137, 553–597, https://doi.org/10.1002/qj.828, 2011. a, b
Doms, G. and Schättler, U.: The nonhydrostatic limited-area model LM (Lokal-Modell) of DWD, Part I: Scientific documentation, Deutscher Wetterdienst (DWD), Offenbach, Germany, 10, 1999. a
Doms, G., Förstner, J., Heise, E., Herzog, H.,Mironov, D., Raschendorfer, M., Reinhardt, T., Ritter, B., Schrodin, R., Schulz, J.-P., and Vogel, G.: A description of the nonhydrostatic regional COSMO model, Part II: Physical parameterization, Deutscher Wetterdienst, Offenbach, Germany, 2011. a, b, c
Gal-Chen, T. and Somerville, R. C.: On the use of a coordinate transformation for the solution of the Navier-Stokes equations, J. Comput. Phys., 17, 209–228, 1975. a
Giorgetta, M. A., Jungclaus, J., Reick, C. H., Legutke, S., Bader, J., Böttinger, M., Brovkin, V., Crueger, T., Esch, M., Fieg, K., Glushak, K., Gayler, V., Haak, H., Hollweg, H-D., Ilyina, T., Kinne, S., Kornblueh, L., Matei, D., Mauritsen,T., Mikolajewicz, U., Müller,W., Notz, D., Pithan, F., Raddatz, T., Rast, S., Redler, R., Roeckner, E., Schmidt, H., Schnur, R., Segschneider, J., D. Six, K., Stockhause, M., Timmreck, C., Wegner, J., Widmann, H., Wieners, K-H., Claussen, M., Marotzke, J., and Stevens, B.: Climate and carbon cycle changes from 1850 to 2100 in MPI-ESM simulations for the Coupled Model Intercomparison Project phase 5, J. Adv. Model. Earth Sy., 5, 572–597, 2013. a
Giorgetta, M. A., Brokopf, R., Crueger, T., Esch, M., Fiedler, S., Helmert, J., Hohenegger, C., Kornblueh, L., Köhler, M., Manzini, E., Mauritsen, T., Nam, C., Raddatz, T., Rast, S., Reinert, D., Sakradzija, M., Schmidt, H., Schneck, R., Schnur, R., Silvers, L., Wan, H., Zängl, G., Stevens, B.: ICON-A, the atmosphere component of the ICON Earth System Model. Part I: Model Description, J. Adv. Model. Earth Sy., 10, 1613–1637, https://doi.org/10.1029/2017MS001242, 2018. a, b
Giorgi, F., Jones, C., and Asrar, G. R.: Addressing climate information needs at the regional level: the CORDEX framework, World Meteorological Organization (WMO) Bulletin, 58, 175 pp., 2009. a
Haylock, M., Hofstra, N., Klein Tank, A., Klok, E., Jones, P., and New, M.: A European daily high-resolution gridded data set of surface temperature and precipitation for 1950–2006, J. Geophys. Res.-Atmos., 113, D20119, https://doi.org/10.1029/2008JD010201, 2008. a, b
Heinze, R., Dipankar, A., Henken, C. C., Moseley, C., Sourdeval, O., Trömel, S., Xie, X., Adamidis, P., Ament, F., Baars, H., Barthlott, C., Behrendt, A., Blahak, U., Bley, S., Brdar, S., Brueck, M., Crewell, S., Deneke,H., Di Girolamo,P., Evaristo, R., Fischer, J., Frank, C., Friederichs, P., Göcke, T., Gorges, K., Hande, L., Hanke, M., Hansen, A., Hege, H-C., Hoose, C., Jahns, T., Kalthoff, N., Klocke, D., Kneifel, S., Knippertz, P., Kuhn, A., van Laar, T., Macke, A., Maurer, V., Mayer, B., Meyer, C. I., Muppa, S. K., Neggers, R. A. J., Orlandi, E., Pantillon, F., Pospichal, B., Röber,N., Scheck, L., Seifert, A., Seifert, P., Senf, F., Siligam, P., Simmer, C., Steinke, S., Stevens, B., Wapler, K., Weniger, M., Wulfmeyer, V., Zängl, G., Zhang, D., and Quaas, J.: Large-eddy simulations over Germany using ICON: A comprehensive evaluation, Q. J. Roy. Meteor. Soc., 143, 69–100, 2017. a
Hofstra, N., Haylock, M., New, M., and Jones, P. D.: Testing E-OBS European high-resolution gridded data set of daily precipitation and surface temperature, J. Geophys. Res.-Atmos., 114, D21101, https://doi.org/10.1029/2009JD011799, 2009. a
Korn, P.: Formulation of an unstructured grid model for global ocean dynamics, J. Comput. Phys., 339, 525–552, 2017. a
Kotlarski, S., Keuler, K., Christensen, O. B., Colette, A., Déqué, M., Gobiet, A., Goergen, K., Jacob, D., Lüthi, D., van Meijgaard, E., Nikulin, G., Schär, C., Teichmann, C., Vautard, R., Warrach-Sagi, K., and Wulfmeyer, V.: Regional climate modeling on European scales: a joint standard evaluation of the EURO-CORDEX RCM ensemble, Geosci. Model Dev., 7, 1297–1333, https://doi.org/10.5194/gmd-7-1297-2014, 2014. a, b, c, d, e
Majewski, D. and Ritter, B.: Das Global-Modell GME, Promet, 27, 111–122, 2002. a
Mlawer, E. J., Taubman, S. J., Brown, P. D., Iacono, M. J., and Clough, S. A.: Radiative transfer for inhomogeneous atmospheres: RRTM, a validated correlated-k model for the longwave, J. Geophy. Res.-Atmos., 102, 16663–16682, 1997. a, b, c
Orr, A., Bechtold, P., Scinocca, J., Ern, M., and Janiskova, M.: Improved middle atmosphere climate and forecasts in the ECMWF model through a nonorographic gravity wave drag parameterization, J. Climate, 23, 5905–5926, 2010. a
Pham, T. V., Brauch, J., Dieterich, C., Früh, B., and Ahrens, B.: New coupled atmosphere-ocean-ice system COSMO-CLM/NEMO: assessing air temperature sensitivity over the North and Baltic Seas, Oceanologia, 56, 167–189, https://doi.org/10.5697/oc.56-2.167, 2014. a
Rieger, D., Köhler, M., Hogan, R., Schäfer, S., Seifert, A., Lozar, A. D., and Zängl, G.: ecRad in ICON – Implementation Overview, Reports on ICON, Deutscher Wetterdienst, Offenbach, Germany, https://doi.org/10.5676/DWDpub/nwv/icon004, 2019. a
Ritter, B. and Geleyn, J.-F.: A comprehensive radiation scheme for numerical weather prediction models with potential applications in climate simulations, Mon. Weather Rev., 120, 303–325, 1992. a
Sanchez-Gomez, E., Somot, S., and Déqué, M.: Ability of an ensemble of regional climate models to reproduce weather regimes over Europe-Atlantic during the period 1961–2000, Clim. Dynam., 33, 723–736, 2009. a
Schär, C., Leuenberger, D., Fuhrer, O., Lüthi, D., and Girard, C.: A new terrain-following vertical coordinate formulation for atmospheric prediction models, Monthly Weather Review, 130, 2459–2480, 2002. a, b, c
Schulz, J.-P., Vogel, G., Becker, C., Kothe, S., Rummel, U., and Ahrens, B.: Evaluation of the ground heat flux simulated by a multi-layer land surface scheme using high-quality observations at grass land and bare soil, Meteorol. Z., 25, 607–620, https://doi.org/10.1127/metz/2016/0537, 2016. a
Stevens, B., Giorgetta, M., Esch, M., Mauritsen, T., Crueger, T., Rast, S., Salzmann, M., Schmidt, H., Bader, J., Block, K., Brokopf, R., Fast, I., Kinne, S., Kornblueh, L., Lohmann, U., Pincus, R., Reichler, T., and Roeckner, E.: Atmospheric component of the MPI-M Earth System Model: ECHAM6, J. Adv. Model Earth Sy., 5, 146–172, https://doi.org/10.1002/jame.20015, 2013. a
Tegen, I., Hollrig, P., Chin, M., Fung, I., Jacob, D., and Penner, J.: Contribution of different aerosol species to the global aerosol extinction optical thickness: Estimates from model results, J. Geophys. Res.-Atmos., 102, 23895–23915, 1997. a
Trusilova, K., Früh, B., Brienen, S., and Keuler, K.: Urban effects in climate simulations for CORDEX Europe, CLM-Community Newsletter, 2, 4–7, 2014. a
Van den Besselaar, E., Haylock, M., Van der Schrier, G., and Klein Tank, A.: A European daily high-resolution observational gridded data set of sea level pressure, J. Geophys. Res.-Atmos., 116, D11110, https://doi.org/10.1029/2010JD015468, 2011. a, b
Zängl, G., Reinert, D., Rípodas, P., and Baldauf, M.: The ICON (ICOsahedral Non-hydrostatic) modelling framework of DWD and MPI-M: Description of the non-hydrostatic dynamical core, Q. J. Roy. Meteor. Soc., 141, 563–579, https://doi.org/10.1002/qj.2378, 2015. a