Synoptic variability of cloud and TOA radiative flux diurnal cycles Patrick Taylor NASA Langley Research Center Climate Science Branch

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Presentation transcript:

Synoptic variability of cloud and TOA radiative flux diurnal cycles Patrick Taylor NASA Langley Research Center Climate Science Branch

Motivation The diurnal cycle is a fundamental earth system variability. Significant diurnal cycle signals are evident in many geophysical datasets, including temperature, water vapor, clouds, radiation, and convective precipitation (e.g., Minnis and Harrison 1984a,b,c; Randall et al. 1991; Janowiak et al. 1994; Bergman and Salby 1996; Lin et al. 2000; Soden 2000; Yang and Slingo 2001). The diurnal cycle is traditionally thought to be the result of a long time average removing “weather noise.”

Background: Diurnal Cycle Regimes Land Ocean ConvectiveNon-Convective Land Ocean Convective and non-convective regimes are determined using climatological High Cloud amount (e.g., Bergman and Salby 1996). Convective: High cloud > 10 % Non-Convective: High cloud < 10 % 9%15% 31%45% Traditional diurnal cycle regimes provide a statistically robust categorization.

Main Points Point 1: The TOA flux (and cloud) diurnal cycle is variable. Point 2: Diurnal cycle variability in TOA flux is driven by clouds. Point 3: Neglecting this variability leads to uncertainty and bias. Point 4: Variability in the diurnal cycle is related to variability in atmospheric dynamic and thermodynamic state. Point 5: Cloud diurnal cycles are sensitive to a sorting by dynamic and thermodynamic conditions.

Diurnal cycle variability defined The monthly, 3-hour composite of a variable differs from month-to-month outside of the random, statistical variations. OLR OLRCLR LWCF TOA flux (W m -2) UTC time

Data CERES SYN Ed2rev1: – Synergistically combines CERES and GEO observations to create a 3-hourly data product by using GEO radiances to obtain diurnal shape and CERES for radiometric accuracy: (1)A calibration of each GEO instrument with MODIS imager data (2)A narrowband radiance to broadband radiance conversion (3)An integration of GEO broadband radiance to irradiance (4)A normalization of GEO derived flux to observed CERES flux. SRB ISCCP Clouds: 1°x1°

Method: Diurnal Harmonic CERES Synoptic Data – 3-hourly CERES-Geo merged data product. Fourier analysis is used to compute diurnal harmonics. LWCF OLR Monthly, 3- hourly composites First Harmonic

OLR Diurnal cycle variability Fourier harmonic analysis is used by fitting a cosine function to monthly, 3-hourly composites of OLR, LWCF, and OLRCLR. The seasonal cycle of the monthly data set is removed and the STDEV is shown here to represent diurnal cycle variability. STDEV(Amplitude) (unit: W m -2 ) STDEV(Phase) (unit: hour)

Alternative diurnal cycle variability metric (RMS) Because of the RSW structure, a Fourier first harmonic fit does not characterize the diurnal cycle well. Therefore, an alternative method is developed to characterize RSW diurnal cycle variability.

RSW diurnal cycle variability: RMS RSW and RMS RSW The RSW diurnal cycle is highly variable in regions of oceanic convection and moderately variable over land convective and ocean non-convective regions. The variability is very small over land non- convective regions. The diurnal cycle variability in the RSW diurnal cycle is entirely due to clouds. SWCF RSW

Assessing uncertainty from neglecting diurnal cycle variability: TOA flux (1)Create a simulated data set with diurnal cycle variability removed. (1)Compare against “truth” data set (CERES SYN Ed2rev1)

Neglecting Diurnal Cycle Variability: Uncertainty OLR RSW Uncertainty in monthly mean OLR and RSW fluxes ranges from 1-7 Wm -2 across the tropics.

Neglecting Diurnal Cycle Variability: OLR Bias OLR’ > +1σ OLR’ < -1σ Systematic bias ranges from +5 to -5 W m -2 when sorted by magnitude of OLR’.

OLR err and RSW err sorted by atmospheric thermodynamic state Shown is the regional difference between OLR sim and OLR obs and RSW sim and RSW obs sorted by the monthly THETA E,SFC anomaly.

OLR err and RSW err sorted by atmospheric dynamic state Shown is the regional difference between OLR sim and OLR obs and RSW sim and RSW obs sorted by the monthly ω 500 anomaly.

South America Convective Region: High Clouds High cloud fraction diurnal cycle amplitude and phase show a sensitivity to CAPE and ω 500 anomalies. CAPEω 500 CAPE’ > +1σ CAPE’ < -1σ ω 500 '> +1σ ω 500 ’< -1σ

South America Convective Region: Low Clouds Low cloud fraction diurnal cycle amplitude and phase show a sensitivity to CAPE and ω 500 anomalies. CAPEω 500 CAPE’ > +1σ CAPE’ < -1σ ω 500 '> +1σ ω 500 ’< -1σ

Main Points Point 1: The TOA flux (and cloud) diurnal cycle is variable. Point 2: Diurnal cycle variability in TOA flux is driven by clouds. Point 3: Neglecting this variability leads to uncertainty and bias. Point 4: Variability in the diurnal cycle is related to variability in atmospheric dynamic and thermodynamic state. Point 5: Cloud diurnal cycles are sensitive to a sorting by dynamic and thermodynamic conditions.

Harmonic vs. RMS Method: OLR These plots present a comparison between the harmonic and RMS diurnal cycle metrics. The same regions are highlighted in both the harmonic and RMS methods. The main point here is that the RMS method cannot distinguish between amplitude and phase contributions. RMS OLR σ AOLR σ POLR

Harmonic vs. RMS Method: LWCF Same as previous but for LWCF. The main point here is that the RMS method cannot distinguish between amplitude and phase contributions. RMS LWCF σ ALWCF σ PLWCF

Neglecting Diurnal Cycle Variability: RSW Bias RSW’ > +1σ RSW’ < -1σ Similar to OLR, systematic bias ranges from +5 to -5 W m -2 when sorted by magnitude of RSW’.

Regional Behavior of OLR and RSW bias Shown is the regional difference between OLR sim and OLR obs and RSW sim and RSW obs sorted by monthly OLR and RSW anomaly, respectively.