1 / 53

Use of ensemble background-error covariances within variational data assimilation for NWP

Use of ensemble background-error covariances within variational data assimilation for NWP. Collaborators: Peter Houtekamer Herschel Mitchell Cecilien Charette Bin He Gerald Desroziers Loik Berre Ron McTaggart-Cowan. Mark Buehner Meteorological Research Division August 1-11, 2011

mreza
Download Presentation

Use of ensemble background-error covariances within variational data assimilation for NWP

An Image/Link below is provided (as is) to download presentation Download Policy: Content on the Website is provided to you AS IS for your information and personal use and may not be sold / licensed / shared on other websites without getting consent from its author. Content is provided to you AS IS for your information and personal use only. Download presentation by click this link. While downloading, if for some reason you are not able to download a presentation, the publisher may have deleted the file from their server. During download, if you can't get a presentation, the file might be deleted by the publisher.

E N D

Presentation Transcript

  1. Use of ensemble background-error covariances within variational data assimilation for NWP Collaborators: Peter Houtekamer Herschel Mitchell Cecilien Charette Bin He Gerald Desroziers Loik Berre Ron McTaggart-Cowan Mark Buehner Meteorological Research Division August 1-11, 2011 LMS - EPSRC Durham Symposium on the Mathematics of Data Assimilation

  2. Contents • Brief description of Canadian operational NWP systems • Description of experimental configurations • Spatial covariance localization • Full analysis-forecast NWP experiments with different approaches for B matrix: • 3D ensemble covariances with spatial localization • 4D ensemble covariances with spatial localization • weighted average of stationary covariances and 3D ensemble covariances with spatial localization • Approach and results from using 3D ensemble covariances with spatial and spectral localization • Conclusions and next steps

  3. Introduction • Goal: examine various approaches for using flow-dependent ensemble-based background error covariances within global deterministic analysis system for operational NWP • Initial project initiated in anticipation of WMO workshop on intercomparison of 4D-Var and EnKF, Buenos Aires, November 2008 • 4D-Var and EnKF: • both operational at CMC since 2005 • both use GEM forecast model • both assimilate similar set of observations using mostly the same observation operators and observation error covariances • current effort towards unifying code of the two systems • 4D-Var is used to initialize medium range global deterministic forecasts • EnKF is used to initialize global Ensemble Prediction System

  4. Operational Systems (up to June 2009) • 4D-Var (Gauthier et al. 2007) • incremental approach: ~35km/150km grid spacing, 58 levels, 10hPa top (now 80 levels, 0.1hPa top) • EnKF (Houtekamer and Mitchell 2005, Houtekamer et al. 2005) • 96 ensemble members (soon 192): ~100km grid spacing, 28 levels, 10hPa top (now 58 levels) • uses 4D background-error covariances to produce 4D analysis (somewhat like 4D-Var, but without TL/AD of forecast model) • assimilates batches of observations sequentially by expliciting solving analysis equation and updating ensemble covariances • additive model error, no covariance inflation

  5. Experimental ConfigurationsModifications relative to 2009 operational systems • Exactly same observations, including conventional data and satellite radiances, assimilated in all experiments • Increased number of levels in EnKF to match 4D-Var • Increased horizontal resolution of 4D-Var inner loop to match EnKF • Other minor modifications in both systems to obtain nearly identical innovations (each tested to ensure no degradation)

  6. Experimental Configurations • Variational data assimilation system (Buehner et al. 2010): • 3D-Var and 4D-Var with stationary B matrix as in operational system: NMC method (Bnmc) • 3D-Var and 4D-Var with flow-dependent B matrix from EnKF with same localization parameters as in EnKF (Benkf) • Ensemble-Var (En-Var): use 4D ensemble covariances to produce 4D analysis without TL/AD models (most similar to EnKF approach) • 3D-Var with B matrix computed as weighted average between Bnmc and Benkf(Bavg) (idea from Hamill and Snyder 2000) • 3D-Var with B matrix from EnKF, but with spatial and spectral localization (Buehner 2011, submitted) • EnKF: Deterministic forecasts initialized with EnKF ensemble mean analysis (requires interpolation from ~100km to ~35km grid)

  7. Experimental Configurations • Variational data assimilation system (Buehner et al. 2010): • 3D-Var and 4D-Var with stationary B matrix as in operational system: NMC method (Bnmc) • 3D-Var and 4D-Var with flow-dependent B matrix from EnKF with same localization parameters as in EnKF (Benkf) • Ensemble-Var (En-Var): use 4D ensemble covariances to produce 4D analysis without TL/AD models (most similar to EnKF approach) • 3D-Var with B matrix computed as weighted average between Bnmc and Benkf(Bavg) (idea from Hamill and Snyder 2000) • 3D-Var with B matrix from EnKF, but with spatial and spectral localization (Buehner 2011, submitted) • EnKF: Deterministic forecasts initialized with EnKF ensemble mean analysis (requires interpolation from ~100km to ~35km grid) Interesting alternative to 4D-Var: doesn’t require development work related to TL/AD of forecast model, lower computational cost if ensemble members already available

  8. Spatial covariance localization(Hamill et al. 2001) • At large separation distances covariances should be small, but estimation error dominates sample covariance estimate • Necessary to reduce distant covariances to reasonably fit large number of observations with only ~100 ensemble members • Severe localization can cause imbalance – more localization required for small ensemble size • Smoothly taper 3D spatial correlations to zero at large separation distance using a Schur product with a positive semi-definite “localization” matrix: B = L◦Bsample • Elements of L typically computed with a function resembling a Gaussian, but reaches zero at finite distance (e.g. 2800km) • For En-Var each 3D block of 4D B matrix is localized in the same way

  9. Spatial localization in variational system(Buehner 2005, Lorenc 2003) • In variational assimilation pre-conditioned with respect to background term, control vector is related to analysis increment by: ∆x = B1/2 ξ • Approach for using ensemble-based B: • no localization: elements of control vector determine global contribution of each normalized ensemble member deviation to the analysis increment: ∆x = ∑kekξk (ξk is a scalar) • spatial localization: elements of control vector determine local contribution of each ensemble member to the analysis increment: ∆x = ∑keko (L1/2ξk) (ξk is a 3D vector, ek is 3D or 4D) • can also combine with standard BNMC matrix (βBens+(1-β)BNMC): ∆x = β1/2 ∑keko (L1/2ξk) + (1-β)1/2 BNMC1/2ξHI • in each case, background cost function Jb is Euclidean inner product: Jb = 1/2 ξT ξ(augmented control vector in case of averaged covariances)

  10. Analysis and Forecast Verification Results En-Var vs. standard approaches and En-Var vs. use of 3D ensemble B matrix En-Varvs. EnKF and En-Var vs. 4D-Var-Bnmc and En-Varvs. 3D-Var-Benkf and En-Varvs. 4D-Var-Benkf

  11. 4D error covariancesTemporal covariance evolution (explicit vs. implicit evolution) EnKF and En-Var: 96 NLM integrations 3D-Var-Benkf only uses these members 4D-Var: 55 TL/AD integrations, 2 outer loop iterations, then 3h NLM forecast -3h 0h +3h “analysis time”

  12. Single observation experimentsDifference in temporal covariance evolution En-Var • radiosonde temperature observation at 500hPa • observation at beginning of assimilation window (-3h) • with same B, increments very similar from 4D-Var, EnKF • contours are 500hPa GZ background state at 0h (ci=10m) + + contour plots at 500 hPa + +

  13. Single observation experimentsDifference in temporal covariance evolution En-Var • radiosonde temperature observation at 500hPa • observation at middle of assimilation window (+0h) • with same B, increments very similar from 4D-Var, EnKF • contours are 500hPa GZ background state at 0h (ci=10m) + + contour plots at 500 hPa + +

  14. Single observation experimentsDifference in temporal covariance evolution En-Var • radiosonde temperature observation at 500hPa • observation at end of assimilation window (+3h) • with same B, increments very similar from 4D-Var, EnKF • contours are 500hPa GZ background state at 0h (ci=10m) + + contour plots at 500 hPa + +

  15. Forecast Results:En-Var vs. EnKF north tropics south Difference in stddev relative to radiosondes: Positive En-Var better Negative  EnKF better En-Var uses incremental approach, deterministic analysis EnKF uses ens. mean at lower resolution zonal wind temp. height

  16. Forecast Results:En-Var vs. 4D-Var-Bnmc north tropics south Difference in stddev relative to radiosondes: Positive En-Var better Negative  4D-Var-Bnmc better zonal wind temp. height

  17. Forecast Results:En-Var vs. 3D-FGAT-Benkf north tropics south Difference in stddev relative to radiosondes: Positive En-Var better Negative  3D-FGAT-Benkf better zonal wind temp. height

  18. Forecast Results:En-Var vs. 4D-Var-Benkf north tropics south Difference in stddev relative to radiosondes: Positive En-Var better Negative  4D-Var-Benkf better zonal wind temp. height

  19. Results – 500hPa GZ anomaly correlation Verifying analyses from 4D-Var with Bnmc Northern hemisphere Southern hemisphere 3D-FGAT Benkf En-Var 4D-Var Benkf 3D-FGAT Benkf En-Var 4D-Var Benkf

  20. Results – 850hPa Temperature bias Verifying analyses from mean of 3 reanalyses (ECMWF, NCEP/NCAR, JMA) 4D-Var-Bnmc 0UTC, 12UTC 6UTC, 18UTC

  21. Results – 850hPa Temperature bias Verifying analyses from mean of 3 reanalyses (ECMWF, NCEP/NCAR, JMA) 4D-Var-Benkf 0UTC, 12UTC 6UTC, 18UTC

  22. Results – 850hPa Temperature bias Verifying analyses from mean of 3 reanalyses (ECMWF, NCEP/NCAR, JMA) En-Var 0UTC, 12UTC 6UTC, 18UTC

  23. Results – Temperature error over N. Africa Verifying analyses from mean of 3 reanalyses (ECMWF, NCEP/NCAR, JMA) Bias StdDev large sensitivity to B at 850hPa over certain areas in the tropics, why? possible problem over land affecting all experiments

  24. Results – Temperature error over N. midlat Verifying analyses from mean of 3 reanalyses (ECMWF, NCEP/NCAR, JMA) Improvement in background state less clear over the northern extra-tropics Bias StdDev

  25. Analysis and Forecast Verification Results Averaged covariances vs. Bnmc and Benkf(similar approach already operational at Met Office) Bavg = ½ Bnmc + ½ Benkf 3D-Var-Bavg vs. 3D-Var-Bnmc and 3D-Var-Bavg vs. 3D-Var-Benkf

  26. Forecast Results:3D-Var-Bavg vs. 3D-Var-Bnmc north tropics south Difference in stddev relative to radiosondes: Positive 3D-Var-Bavg better Negative  3D-Var-Bnmc better zonal wind temp. height

  27. Forecast Results:3D-Var-Bavg vs. 3D-Var-Benkf north tropics south Difference in stddev relative to radiosondes: Positive 3D-Var-Bavg better Negative  3D-Var-Benkf better zonal wind temp. height

  28. Results – 500hPa GZ anomaly correlation Verifying analyses from 4D-Var with Bnmc Northern hemisphere Southern hemisphere Benkf0.50and0.75 are best Benkf0.75and 1.00 are best Bnmc and Benkf 1.00 worst Bnmc worst Bnmc Benkf 0.25 Benkf 0.50 Benkf 0.75 Benkf 1.00

  29. Comparison of several approaches for using ensemble correlations (Buehner 2011, submitted) • During visit to Meteo-France, compared several approaches for using ensemble-based covariances in a variational assimilation system: • spatial localization (standard Schur product approach): B = L◦Bsample • wavelet diagonal (as developed and used at ECMWF): B = W-1diag(WBsampleWT) W-T • spectral diagonal (homogeneous/isotropic correlations): B = S-1diag(SBsampleST) S-T also variances averaged for each n • new spatial/spectral localization approach that combines aspects of spatial localization and wavelet diagonal approaches: B = ΣjLj◦(WjBsampleWjT) spatial localization and diagonal wrt scale j ***new approach allows scale-dependent spatial localization***

  30. Spatial/Spectral correlation localization • In variational assimilation pre-conditioned with respect to background term, control vector is related to analysis increment by: ∆x = B1/2 ξ • Approach for using ensemble-based B: • spatial localization: elements of control vector determine local contribution of each ensemble member to the analysis increment: ∆x = ∑keko (L1/2ξk) (ξk is a 3D vector) • spatial/spectral localization: elements of control vector determine local contribution of each ensemble member for a particular horizontal scale: ∆x = ∑j∑kek,jo (Lj1/2ξk,j) where ek,j = Wjek = S-1ΨjS ek • could also be used in EnKF

  31. Spatial/Spectral correlation localization • In variational assimilation pre-conditioned with respect to background term, control vector is related to analysis increment by: ∆x = B1/2 ξ • Approach for using ensemble-based B: • spatial localization: elements of control vector determine local contribution of each ensemble member to the analysis increment: ∆x = ∑keko (L1/2ξk) (ξk is a 3D vector) • spatial/spectral localization: elements of control vector determine local contribution of each ensemble member for a particular horizontal scale: ∆x = ∑j∑kek,jo (Lj1/2ξk,j) where ek,j = Wjek = S-1ΨjS ek • could also be used in EnKF 3D field for each scale and each member wavelet functions: overlapping band-pass spectral filter

  32. Spatial/Spectral correlation localizationEffective wavenumber localization matrix wavelet functions used for wavelet diagonal approach • making correlations diagonal with respect to wavelet bands causes spectral localization • spectral localization is equivalent to local spatial averaging of correlation functions more severe localization causes spatial averaging over a larger area • extent of spectral localization governed by choice of wavelet functions wavelet functions used for new spatial/spectral localization approach

  33. Spatial/Spectral correlation localizationMeasuring correlation estimation error for each spectral band n=032 n=165 • mean correlation and estimation error as function of separation distance for different spectral bands • compute covariance between 2 independent samples: “agreement” • for higher wavenumber bands: • average correlation sharper (no surprise) • large estimation error begins at shorter separation distance • therefore could benefit from more severe spatial localization: scale-dependent spatial localization n=3498 n=6799 note: estimation error is large when agreement < magnitude n=099

  34. Spatial/Spectral correlation localization • idealized experiments with “true” correlations produced from 96-member EnKF ensemble of 500hPa temperature with weak spatial localization • 48-member random ensemble generated using “true” correlations and each approach applied • with new approach, less spatial localization applied to large scales than small scales: scale-dependent localization

  35. Spatial/Spectral correlation localization • zonal correlation length scale computed using Daley’s definition: (-d2c/dx2)-1/2 • finite difference approximation for second derivative centered on origin of each correlation function

  36. Spatial/Spectral correlation localization • rms error of each correlation estimate averaged over all separation distances (up to 3000km) and over many locations over North America

  37. Spatial/Spectral correlation localization raw sample raw sample and truth • mean correlation and error stddev of correlations as a function of separation distance • spatial/spectral localization and wavelet diagonal approaches do not reproduce variance of 1 everywhere (possibly due to uneven spectral localization)

  38. Spatial/Spectral correlation localization Impact of using scale-dependent localization • mean correlation and error stddev of correlations as a function of separation distance • solid = scale-dependent localization (3500km, 3000km, 2500km, 2000km) • dashed = scale-independent localization (3000km) similar error stddev with scale-dependence smaller negative bias with scale-dependence truth

  39. Spatial/Spectral correlation localization • single observation of 500hPa temperature near region of strong north-westerly winds • temperature increment = shading • wind increment = vectors • background 500hPa geopotential height = contours

  40. Spatial/Spectral correlation localization • single observation of 500hPa temperature near region of strong north-westerly winds • temperature increment = shading • wind increment = vectors • background 500hPa geopotential height = contours

  41. Spatial/Spectral correlation localization 1-month 3D-Var data assimilation experiments • initial value of radiosonde cost function shows that spatial/spectral localization produces better analyses than with spatial localization only • scale-dependent spatial localization better than using same spatial localization for all scales Initial value of Jraob

  42. Spatial/Spectral correlation localization 1-month 3D-Var data assimilation experiments • 48h forecasts from using a B matrix estimated from: • grey: 96 ensemble members with spatial localization only • black: 48 ensemble members with spatial localization only

  43. Spatial/Spectral correlation localization 1-month 3D-Var data assimilation experiments • 48h forecasts from using a B matrix estimated from: • grey: 96 ensemble members with spatial localization only • black: 48 ensemble members with spatial localization and spectral localization over 6 evenly spaced total wavenumber bands

  44. Spatial/Spectral correlation localization 1-month 3D-Var data assimilation experiments • 48h forecasts from using a B matrix estimated from: • grey: 96 ensemble members with spatial localization only • black: 48 ensemble members with spatial localization and spectral localization over 6 evenly spaced total wavenumber bands, scale-dependent spatial localization

  45. Conclusions • En-Var approach is attractive possible alternative to 4D-Var and current EnKF sequential* analysis approach (*wrt batches of observations) • advantages of En-Var vs. full 4D-Var: • no need to maintain TL/AD version of model dynamics and physical parameterizations (EnKF members already available) • more computationally efficient and likely easier to parallelize for high spatial resolution and large data volumes • potential advantages from using En-Var within EnKF instead of current approach: • global analysis (all obs treated together – don’t have to perform all analyses in parallel) • localization of B instead of BHT (latter is a potential problem for non-local observations: satellite radiances) • allows use of alternative approaches for modelling covariances: e.g. averaged covariances • allows use of variational quality control

  46. Next Steps • Test En-Var approach in operational configuration of deterministic prediction system to compare with 4D-Var (requires raising top level of EnKF to 0.1hPa and synchronization in development of the two systems) • Examine possibility of using a variational approach for EnKF analysis step (i.e. can En-Var be made efficient enough to perform 192 analyses in < 1 hour? Or can we use less members with En-Var than EnKF? Can the minimizations work together?--Gerald’s talk) • Continue to modularize/unify the code for Variational and EnKF data assimilation systems to facilitate further development of both systems and hybrid approaches as described above

  47. References Buehner, M., 2005, "Ensemble-derived stationary and flow-dependent background error covariances: Evaluation in a quasi-operational setting for NWP ." Quart. J. Roy. Meteor. Soc. Vol. 131, p1013-1044. Buehner, M., P.L. Houtekamer, C. Charette, H.L. Mitchell, B. He, 2010, "Intercomparison of variational data assimilation and the Ensemble Kalman Filter for global deterministic NWP. Part I: Description and Single-Observation experiments." Monthly Weather Review. Vol. 138, p1550-1566. Buehner, M., P.L. Houtekamer, C. Charette, H.L. Mitchell, B. He, 2010, "Intercomparison of variational data assimilation and the Ensemble Kalman Filter for global deterministic NWP. Part II: One-Month Experiments with Real Observations." Monthly Weather Review. Vol. 138, p1567-1586. Gauthier, P., M. Tanguay, S. Laroche, S. Pellerin, J. Morneau, 2007, “Extension of 3DVAR to 4DVAR: Implementation of 4DVAR at the Meteorological Service of Canada.” Mon. Wea. Rev., Vol 135, p2339–2354. Hamill, T. M. and Snyder, C. 2000 A hybrid ensemble Kalman filter—3D variational analysis scheme. Mon. Weather Rev., Vol. 128, p2905–2919. Hamill, T. M., Whitaker, J. S. and Snyder, C. 2001 Distance-dependent filtering of background error covariance estimates in an ensemble Kalman filter. Mon. Weather Rev., Vol. 129, p2776–2790 Houtekamer, P. L., H. L. Mitchell, G. Pellerin, M. Buehner, M. Charron, L. Spacek and B. Hansen, 2005, "Atmospheric data assimilation with the ensemble Kalman filter: Results with real observations ." Monthly Weather Review, Vol. 133, p604-620. Houtekamer, P. L., and H. L. Mitchell, 2005, “Ensemble Kalman filtering.” Quarterly Journal of the Royal Meteorological Society, Vol 131, p3269–3289 Houtekamer, P. L., H. L. Mitchell, X. Deng, 2009, “Model Error Representation in an Operational Ensemble Kalman Filter.” Monthly Weather Review. Vol 137, p2126-2143. Lorenc, A. C. 2003 The potential of the ensemble Kalman filter for NWP: A comparison with 4D-Var. Q. J. R. Meteorol. Soc., Vol. 129, p3183–3203.

  48. Extra Slides Follow

  49. Forecast Results:En-Var vs. EnKF north tropics south Significance level of difference in stddev relative to radiosondes: Positive En-Var better Negative  EnKF better zonal wind temp. Computed using bootstrap resampling of the individual scores for 48-hour non-overlapping periods. height Shading for 90% and 95% confidence levels

  50. Forecast Results:En-Var vs. 4D-Var-Bnmc north tropics south Significance level of difference in stddev relative to radiosondes: Positive En-Var better Negative  4D-Var-Bnmc better zonal wind temp. Computed using bootstrap resampling of the individual scores for 48-hour non-overlapping periods. height Shading for 90% and 95% confidence levels

More Related