Norwegian Climate Prediction Model

The Norwegian Climate Prediction Model (NorCPM) is aiming at providing prediction from seasonal-to-decadal time scale. It is based on the Norwegian Earth System Model (NorESM, [1]) and the Ensemble Kalman Filter (EnKF, [2]) data assimilation method. NorESM is a state of the art Earth system model that is based on CESM ([3]), but uses a different aerosol/chemistry scheme and ocean model (evolved from MICOM). The EnKF is a sequential data assimilation method that allows for fully multivariate and flow dependent corrections using a covariance matrix produced by a Monte-Carlo ensemble integration.

NorESM model version used in NorCPM

NorESM1-L (Zhang et al., 2012) T31 resolution in the atmosphere; ocean is bipolar gx3v7 (~3°).
NorESM1-LT ([Wang et al. 2017 Kimmritz et al. 2018) atmosphere has a resolution of 1.9°x2.5° and ocean has a resolution of 1° with a tripolar grid.
BCCRFAST tripolar (Gao et al. 2018 atmosphere has a resolution of 1.9°x2.5° ocean is tripolar 1°.
NorESM1-ME (Bentsen et al. 2013,Tjiputra et al., 2013) atmosphere has a resolution of 1.9°x2.5° ocean has a 1° resolution.
NorESM1-ACPL (Toniazzo and Koseki 2018) atmosphere has a resolution of 1.9°x2.5° ocean has a 1° resolution anomaly coupled ocean atmosphere. Anomaly coupling modifies coupling fields by a fixed seasonal climatological correction, such that biases in SSTs and surface wind stress are obviated.
NorESM2-MH (Langehaug et al. 2018) atmosphere has a resolution of 1° ocean has a resolution of 1/4°.

NorCPM Versions

FREE: refers to an ensemble simulation of NorESM carried without assimilation and starting from the same initial ensemble than the assimilation experiment. The initial ensemble is generated by spinning up an ensemble of states (sampled from a long preindustrial forcing run) with real historical forcing from 1850. Such experiment provides a benchmark for data assimilation and is also used to disentangle the part of prediction skill related to natural internal variability from the part driven by external forcing.
Version 0 (V0): refers to version of NorCPM that assimilate SST only. SST is the only observational data set available in the ocean for a period of time sufficient (> 100 years) to clearly demonstrate skill of decadal prediction. Assimilation updates vertically the full ocean while the remaining components of the Earth system model (atmosphere, sea ice, land) are left unchanged but they will adjust dynamically between the monthly assimilation step (an approach referred as weakly coupled data assimilation).

V0 was first tested in idealised twin experiment (Counillon et al. 2014). It is found that assimilation reduces error and can constrain well the variability of the ocean – with largest improvements in the near surface and sea ice with some benefit over land for temperature and precipitation. The system beats persistence forecast and shows skill for the heat content in the Nordic Seas that is close to the upper predictability limit.

V0 was tested in a real framework and a long stochastic reanalysis was produced for the period 1950—2010 which assimilates the anomaly of the HadiSST2 within the period 1950-2010. provides a

stochastic reconstruction of SST � that is, providing a three-dimensional estimate of the measurement and its accuracy �for the period 1850�2010. A method referred to as upscaling (Wang et al. 2016) is used to ensure that the assimilation does not introduce a drift when updating the non-Gaussian distributed layer thickness variables. The system can reproduce well the North Atlantic variability and shows good agreement with independent objective analysis of the oceanic heat content and salt content globally. It was noted that using a flow dependent data assimilation method and formulating the ocean covariance in isopycnal coordinates are important ingredient for efficiently propagating the surface information below the mixed layer in the Labrador Sea and to constrain the formation of deep water convection.

In Wang et al. (sub) hindcasts are started from a shorter reanalysis (started in 1980) reanalysis. The system shows highly competitive skill compared to North American multi-model ensemble and skilful skill for sea ice extent were variability is driven by ocean variability (e.g. in the boreal winter in the Barents Sea, ….). The skill of decadal hindcasts were tested for 1955:2010. There are some skill for prediction of AMO and AMOC at 26 but the prediction of the SPG is poor despite a very good match during the reanalysis. Bethke et al. in prep identified that the reason for the poor forecast is a combined effect of a bias in the deep subtropical region and a wrong salinity update in the SPG region.

Version 1 (V1): the system is complemented with the assimilation of hydrographic profiles. Assimilating observations in an isopycnal coordinate model is not strait forward as the observation operator must interpolate either from isopycnal corodinates to z coordinates or vice versa. In Wang et al. 2016 it is shown that the approach to interpolate the model onto z coordinates (still keeping the covariance in isopycnal coordinates) is more linear than interpolating the observations to isopycnal coordinates and as such more efficient. Practical implementations of localisation and the representation error were extensively tested and version 1 has been run with optimal setting. The system is shown to be able to constrain well the error in the interior while being reliable. The performance of the prediction was tested for the period 1980-2017 in real framework with anomaly assimilation. While complementing the system with hydrographic profile yields little benefit on seasonal time scale, it greatly enhances the skill for decadal predictions in the SPG region (Bethke et al. in prep). There are currently different version of V1. In V1a, all ocean observations are kept and we do not update the sea ice compartment during assimilation. In V1b, we reject observation if it is located in places where there is ice (This run performs poorer than V1a). In v1c all observations are retained but error of TS profiles error is inflated by a factor of 3 because there is large uncertainty for the climatology there (with anomaly assimilation). We also update the sea ice compartment (strongly coupled DA). Most difference between v1a, v1b and v1c is in sea ice covered region and v1c is performing best there. V1c is the version that would be used by default in CMIP6 DCPP.

Version 2 (V2): the system is complemented with assimilation of sea ice concentration. In Kimmritz et al. 2018, we tested different implementations of the data assimilation system in an idealised twin experiment. It is shown that a joint update of the ocean and the sea ice state during the assimilation is beneficial (strongly coupled data assimilation) with a flow dependent covariance method. It is also strongly beneficial to include the different thickness categories in the state vector. Assimilation is able to constrain well errors in sea ice and in the near surface ocean. The method is tested in real framework in Kimmritz et al. in prep. The system show reduced error for sea ice thickness. Prediction of sea ice extent are also greatly enhance in many regions were sea ice yields predictability.

For each of the NorCPM version the assimilation are either carried using full field assimilation or anomaly assimilation. In full field assimilation the observations are assimilated as they are. An advantage of that approach is that it constrains the model bias, but there is a risk that models are attracted to their bias climatology. In such a case, the redundant corrections will transfers the bias from the observed variables to the non observed variables via the covariance during assimilation. In anomaly assimilation the anomaly of model and observation are calculated from their respective seasonal climatology before they are compared. As a consequence, bias are left as they are and we aim only at synchronising the variability. This approach also has some drawback as bias in the mean state also yields two a bias in the variability (for example if the Gulf Stream is misplaced). Carrassi et al. 2014 details the advantage and inconvenient of both approach.

Projects funding the NorCPM activities

Current:NFR-SFE (2018-2021), EU-Blue-Action (2016-2019), Norforsk-ARCPATH (2016-2020), NFR-SNOWGLACE (2015-2018), EU-INTAROS (2016-2020), BFS-BCPU(2018-2021); EU-TRIATLAS(2019-2024)
Completed:NFR-EPOCASA (2014-2017), EU-PREFACE (2014-2017), SKD-PARADIGM (2015-2017), SKD- INCREASE (2015-2017), SKD-PRACTICE (2012-2015)

NorCPM activities received a grant for computer time from the Norwegian Program for supercomputer (NOTUR2, project number NN9039K) and a storage grant (NORSTORE, NS9039K).

Publications, etc.

1. Counillon, F., Bethke, I., Keenlyside, N., Bentsen, M., Bertino, L., & Zheng, F. (2014). Seasonal-to-decadal predictions with the ensemble Kalman filter and the Norwegian Earth System Model: a twin experiment. Tellus A, 66. doi:10.3402/tellusa.v66.21074
2. Wang Y, Counillon F, Bertino L. Alleviating the bias induced by the linear analysis update with an isopycnal ocean model. Quarterly Journal of the Royal Meteorological Society. 2016. https://doi.org/10.1002/qj.2709
3. Counillon F, Keenlyside N, Bethke I, Wang Y, Billeau S, Shen M-L, et al. Flow-dependent assimilation of sea surface temperature in isopycnal coordinates with the Norwegian climate prediction model. Tellus. Series A, Dynamic meteorology and oceanography. 2016;68:32437.
4. Gleixner S.; Keenlyside N.; Dimissie T., Counillon F., Wang Y.; Viste E. Seasonal predictability of Kiremt rainfall in CGCMs, Environmental Research Letters 2017.
5. Wang Y, Counillon F, Bethke I, Keenlyside N, Bocquet M, Shen M-L. Optimising assimilation of hydrographic profiles into isopycnal ocean models with ensemble data assimilation. Ocean Modelling. 2017;114.
6. Kimmritz M., Counillon F., Bitz C.M., Massonnet F., Bethke I., Gao Y. Optimising assimilation of sea ice concentration in an Earth system model with a multicategory sea ice model, Tellus A., 2018
7. Wang et al. Seasonal predictions initialised by assimilating sea surface temperature observations with the EnKF, submitted
8. Kimmritz et al. Added value of sea ice assimilation for seasonal prediction in the Arctic, in prep
9. Jackson et al. North Atlantic circulation: a perspective from ocean reanalyses.
10. Bethke et al. Impact of subtropical North Atlantic initialisation errors on subpolar gyre prediction in prep.
11. Ogawa et al. Arctic sea ice has no influence on AO/NAO, in prep.
12. Counillon et al. Relating model bias and prediction skill in the tropical Atlantic, in prep.
13. Fransner et al. What yields predictability of biochemistry for seasonal to decadal time scale, in prep.

NorCPM is contribution to the WMO Lead Centre for Annual-to-Decadal Climate Prediction under the name BCCR. We intend to contribute to CMIP6 DCPP.

User Resources

All the code for running the system is available on GitHub. The repository is private so please request to an account to access it. [https://github.com/BjerknesCPU/NorCPM]

Contact informations

Leader Prof. Noel Keenlyside;
NorESM related questions Dr. Ingo Bethke, Alok Gupta;
Data assimilation related questions Dr. François Counillon, Dr. Yiguo Wang;
Sea ice prediction Dr. Madlen Kimmritz, Dr. François Counillon
Atmospheric nudging Dr. Mao-Lin Shen, Dr. Fei Li;
Biochemistry predictions Dr. Filippa Fransner

Existing runs

Following is a table that summarise the different experiment runs available so far:

All data are available on Norwegian storage facilities NIRD norwegian . All path below are given relative to the path /projects/NS9039K/shared/norcpm/cases/NorCPM/

Reanalysis

Name	NorESM version	full_field/anom	NorCPM version	Obs data set	ens size	assim freq	period	forcing	var updated	localisation	Path	Publications using it
Reana_twin_PI	NorESM1-L	full_field	V0	Micom SST	30	monthly	610-710	PI	ocn(all)	poin hor. no vert	tape	Counillon et al. 2014
Free_PI	NorESM1-L	FREE	-	-	30	-	610-710	PI	-	-	tape	Counillon et al. 2014
Free_NorESM1	NorESM1-ME	FREE	-	-	30	-	1850-2010	CMIP5 hist	-	-	../NorESM1-ME_historicalExt_noAssim/	Counillon et al. 2016
Reana-V0-long	NorESM1-ME	anom	V0	HadiSST2	30	monthly	1950-2010	CMIP5 hist	ocn(all)	poin hor. no vert	True_Obs-1950-2010/ME/	Counillon et al. 2016, Bethke et al. in prep
Reana-V0-short	NorESM1-ME	anom	V0	HadiSST2	30	monthly	1980-2010	CMIP5 hist	ocn(all)	30 obs	True_Obs-1980-2000/ana_19800115_me/	Wang et al. sub
Reana-bccrfast	BCCRFAST	anom	V0	HadiSST2	30	monthly	1950-2010	CMIP5 hist	ocn(all)	poin hor. no vert	ana_19500115_bccrfast	none
Reana-bccrfast_v1	BCCRFAST	anom	V1	HadiSST2+EN4.1 profiles	30	monthly	1980-2010	CMIP5 hist	ocn(all)	Wang et al 2017, no vert	ana_19791115_bccrfast_SSTTS	none
Free_bccrfast	BCCRFAST	FREE	-	-	30	-	1850-2010	CMIP5 hist	-	-	../bccr-fast_historical_18500101/	none
Reana-v1a	NorESM1-ME	anom	V1	Hadisst2+EN4.1 profiles	30	monthly	1980-2010	CMIP5 hist	ocn(all)	Wang et al 2017, no vert	NorCPM_V1/ana_19800115_me/	Jakson et al. in prep, Bethke et al. in prep
Reana-v1-F	NorESM1-ME	full-field	V1	Hadisst2+EN4.1 profiles	30	monthly	2000-2010	CMIP5 hist	ocn(all)	Wang et al 2017, no vert	tape	Wang et al. 2017
Reana-V1-bccrfast	BCCRFAST	anom	V1	Hadisst2+EN4.1 profiles	30	monthly	1980-2010	CMIP5 hist	ocn(all)	Wang et al 2017, no vert	ana_19791115_bccrfast_SSTTS	none
Reana-V0-bccrfast	BCCRFAST	anom	V0	Hadisst2	30	monthly	1950-2010	CMIP5 hist	ocn(all)	Wang et al 2017, no vert	ana_19500115_bccrfast	none
SFE	NorESM1-ME	anom	V1	NOAA-SST+EN4.2 profiles	30	monthly	2006-present	CMIP5 hist	ocn(all)	Wang et al 2017, no vert	True_Obs-2006-2017/reanalysis/	none
Reana-acpl	NorESM1-acpl	anom	V1	Hadisst2+EN4.1 profiles	30	monthly	1980-2010	CMIP5 hist	ocn(all)	Wang et al 2017, no vert	Anomaly_coupled/	Counillon et al. in prep
Free_twin_V2	NorESM1-LT	FREE	-	-	30	-	1000-1020	PI	-	-	Twin_experiment/TWIN_Free	Kimmritz et al. 2018
Reana_twin_V2	NorESM1-LT	full field	V2	micom_icec	30	monthly	1000-1020	PI	ocn(all) + ice(all)	800 km	Twin_experiment/TwinA56/	Kimmritz et al. 2018
Reana-v2-F	NorESM1-ME	full field	V2	Hadisst2+EN4.1 profiles	30	monthly	1980-2010	CMIP5 hist	ocn(all) + ice(all)	Wang et al 2017, no vert, 800 km	NorCPM_V2/ana_me_ICEC-SST-S-T-1980-2010/
Reana-v2-a	NorESM1-ME	anom	V2	Hadisst2+EN4.1 profiles	30	monthly	1980-2010	CMIP5 hist	ocn(all) + ice(all)	Wang et al 2017, no vert, 800 km	NorCPM_V2a/ana_me_ICEC-SST-S-T-1980-2010/	Kimmritz et al. in prep, Ogawa et al. in prep
Reana-v1b	NorESM1-ME	anom	V1	Hadisst2+EN4.2 profiles; masked in sea ice	30	monthly	1980-2010	CMIP5 hist	ocn(all)	Wang et al 2017, no vert	NorCPM_V1b/ana_19800115_me/	Ogawa et al. in prep
Reana-v1c	NorESM1-ME	anom	V1	Hadisst2+EN4.2 profiles	30	monthly	1980-2010	CMIP5 hist	ocn(all)+ice(all)	Wang et al 2017, no vert	NorCPM_V1c/ana_19800115_me/

Hindcats

Name	Reana used	length	Model	period	frequency	enssize	path	papers
Dec-hind-V0	Reana-V0	10 years	NorESM1-ME	1955-2010	Every 2 years	20	True_Obs-1950-2010/ME_hindcasts/	Bethke et al. in prep
seas-hind-V2F	Reana-v2-F	13 months	NorESM1-ME	1985-2010	4 times per year	9	NorCPM_V2/SeasHind_ana_me_ICEC-SST-S-T-1985-2010/	none
seas-hind-V2a	Reana-v2-a	13 months	NorESM1-ME	1985-2010	4 times per year	9	NorCPM_V2a/hindcast/	Kimmritz et al. in prep
Dec-hind-V1a	Reana-V1a	10 years	NorESM1-ME	1985-2010	Every 2 years	5	NorCPM_V1/ana_19800115_me_dec_19851015/	Bethke et al. in prep
seas-hind-V1a	Reana-V1a	13 months	NorESM1-ME	1985-2010	4 times per year	5	NorCPM_V1/ana_19800115_me_hindcasts/	Wang et al. in prep
seas-hind-V1b	Reana-V1b	13 months	NorESM1-ME	1985-2010	4 times per year	5	NorCPM_V1b/ana_19800115_me_hindcasts/
seas-hind-V1c	Reana-V1b	13 months	NorESM1-ME	1985-2017	4 times per year	5	NorCPM_V1c/ana_19800115_me_hindcasts/
seas-hind-acpl	Reana-acpl	13 months	NorESM1-ME	1985-2017	4 times per year	5	Anomaly_coupled/acpl_19800115_me_hindcasts_*	Counillon et al. in prep