Last modified on Mar 14, 2022 16:53

Contributors: Johannes Mayer, Michael Mayer, Leopold Haimberger

Acronyms

Introduction

Executive Summary

This dataset provides monthly means of mass-consistent atmospheric energy and moisture budget terms derived from 1-hourly ERA5 reanalysis data using advanced numerical and diagnostic methods. Mass consistency is achieved by iteratively adjusting the wind field every time step. This dataset allows to evaluate atmospheric energy and moisture budget diagnostics for the period from 1979 onward. 

Scope of Documentation

This documentation describes the computation of mass-consistent budget terms using 1-hourly analysed state quantities from ERA5.

Version History

No previous versions.

Product Description

Product Overview

Data Description

 Table 1: Dataset general attributes

Table 2: Variables summary

Table 3: versions history

Input Data

Table 4: Input datasets

Method

Background

All ERA5 input fields are transformed (for details see below) to a full Gaussian grid F480 (quadratic grid with respect to the native spectral resolution T639) to avoid aliasing effects. Vorticity and divergence are used to compute the horizontal wind vector at each atmospheric level. Before individual budget terms are computed, the three-dimensional wind field is iteratively adjusted according to the diagnosed imbalance between divergence of vertically integrated dry mass flux and tendency of dry air.  This procedure is repeated every time step. 

Mass Adjustment

Mass-consistent wind fields are obtained by computing the residual of the mass continuity of dry air, which reads as follows

\( \begin{equation} Re = \nabla \cdot \dfrac{1}{g} {\displaystyle\int_0^{p_S}} \left[(1 - q)\vec{v}\right] \; dp + \dfrac{1}{g} \dfrac{\partial}{\partial t} {\displaystyle\int_0^{p_S}} (1 - q) \; dp, \end{equation} \)

where g is the gravitational acceleration, p_S is the surface pressure, q is the specific humidity, and \vec{v} is the horizontal wind vector. The first term on the right side is the divergence of vertically integrated dry mass flux, and second term describes the surface pressure tendency induced by dry air. Inverting the Laplacian of Re and taking the gradient yields a vertically integrated erroneous mass flux, which is converted to a two-dimensional spurious wind field. This spurious divergent wind is subtracted from the original wind field at each level (barotropic wind field correction) making it consistent with the analyzed mass tendency of dry air. After a second iteration of this procedure, mass-adjusted wind fields are used to compute atmospheric energy and moisture budget terms. 

Atmospheric Energy Budget

Atmospheric energy fluxes and tendencies are computed according to a simplified version of the energy budget as proposed  by Mayer et al. (2017), where vertical and lateral enthalpy fluxes associated with water and snow are consistently neglected, such that

\( \begin{equation} F_{TOA} - \underbrace{\nabla\cdot \dfrac{1}{g} {\displaystyle \int_0^{p_S}} [ (1 - q) c_p T_c + L_v (T_c) q + \Phi + k] \; \vec{v}\; dp}_{\text{tediv} = \nabla\cdot (\text{tefle, tefln})^T} - \underbrace{\dfrac{\partial}{\partial t} \dfrac{1}{g}  {\displaystyle\int_0^{p_S}} [ (1 - q) c_v T_c + L_v (T_c) q + \Phi + k] dp}_{\text{tetend}} - F_S = 0 \end{equation} \)

where c_p is the specific heat capacity of dry air at constant pressure, T_c is the air temperature measured in Celsius, L_v(T) is the temperature-dependent latent heat of vaporization, Φ is the potential energy, k is the kinetic energy, and c_v is the specific heat capacity of dry air at constant volume. The vertical fluxes F_TOA and F_S describe the net energy flux at the top of the atmosphere and the net surface heat (radiative + turbulent) flux, which are both not included in this dataset. The second term describes the divergence of vertical integral of atmospheric moist static plus kinetic energy flux (i.e., the divergence of north- and westward atmospheric energy fluxes), and the third term describes the tendency of vertical integral of atmospheric total energy, with the internal energy c_vT_c. The temperature-dependent latent heat of vaporization is computed according to the IFS documentation, Part IV, and is defined as 

\( L_v(T_c) = L_v(T_0) + (c_{pv} - c_l)*(T - T_0), \)

where L_v(T₀) = 2.5008x10⁶ J kg^-1  is the latent heat at the triple point temperature T₀ (in Kelvin), c_pv is the specific heat capacity of water vapour at constant pressure, c_l is the specific heat of liquid water, and T is the air temperature measured in Kelvin. To derive energy budget terms with constant latent heat of vaporization (as provided by ERA5), latent heat terms can be subtracted and replaced by corresponding water vapour terms multiplied by  L_v(T₀).  The potential energy Φ is computed as described in the IFS documentation, Part III.

Atmospheric Moisture Budget

The atmospheric moisture budget can be written as

\( \underbrace{\nabla \cdot \dfrac{1}{g} {\displaystyle\int_0^{p_S}} (q \vec{v}) \; dp}_{\text{wvdiv}} + \underbrace{\dfrac{1}{g} \dfrac{\partial}{\partial t} {\displaystyle\int_0^{p_S}} q \; dp}_{\text{wvtend}} + P + E = 0, \)

where precipitation P and evaporation E (not in this dataset) are surface mass fluxes in units kg m^-2 s^-1.  The first term describes the divergence of vertical integral of atmospheric water vapour flux, the second term describes the tendency of vertical integral of atmospheric water vapour (i.e., total column vapour). That is, atmospheric fluxes and tendencies of water vapour must balance surface freshwater fluxes P+E. Note that the divergence term of the moisture budget also employs mass-adjusted wind fields \vec{v}, albeit it is effected only weakly by spurious divergent winds. 

Model / Algorithm

The following pseudo code describes the mass-adjustment procedure and subsequent computation of energy and moisture budget terms. All spectral transformations (i.e., gradient and divergence computations, Laplace inversion) were performed with routines from OpenIFS .  

\( \begin{align} &\text{for each time step do } \\ &\qquad \Phi_S \leftarrow \text{ read surface geopotential} \\ &\qquad vort \: \leftarrow \text{ read vorticity} \\ &\qquad div \;\;\; \leftarrow \text{ read divergence} \\ &\qquad T \;\;\;\;\;\;\; \leftarrow \text{ read temperature} \\ &\qquad q \;\;\;\;\;\;\;\: \leftarrow \text{ read specific humidity} \\ &\qquad p_S \;\;\;\;\: \leftarrow \text{ read logarithm of surface pressure} \\ &\qquad tcwv \leftarrow \text{ read total column water vapour} \\ &\qquad \\ &\qquad \text{Transform input fields to full Gaussian grid F480} \\ &\qquad \\ &\qquad \vec{v} \leftarrow \text{ compute horizontal wind field using } vort, div \\ &\qquad qtend \;\;\leftarrow \text{ compute tendency of total column water vapour using } tcwv \\ &\qquad mtend \leftarrow \text{ compute tendency of vertically integrated atmospheric mass using } p_S \\ &\qquad \\ &\qquad \text{for each correction step do } \\ &\qquad\qquad mdiv \;\;\;\leftarrow \text{ compute divergence of vertically integrated dry mass flux using } \vec{v} \\ &\qquad\qquad wvdiv \;\leftarrow \text{ compute vertically integrated water vapour divergence using } \vec{v}, q \\ &\qquad\qquad errdiv \leftarrow mdiv - wvdiv + mtend - qtend \\ &\qquad\qquad \vec{v}_{err} \;\;\;\;\;\; \leftarrow \text{ compute spurious two-dimensional wind field using } errdiv \\ &\qquad\qquad \text{ for each atmospheric level } i \text{ in } \vec{v} \text{ do } \vec{v}_i \leftarrow \vec{v}_i - \vec{v}_{err} \\ &\qquad \text{end do} \\ &\qquad \\ &\qquad T_c \leftarrow T - 273.15 \\ &\qquad lhtend \;\;\leftarrow \text{ compute tendency of vertical integral of atmospheric latent heat using } q, T_c \\ &\qquad tetend \;\;\leftarrow \text{ compute tendency of vertical integral of atmospheric total energy using } \vec{v}, q, T_c, \Phi_S \\ &\qquad wvtend \leftarrow \text{ compute tendency of vertical integral of atmospheric water vapour using } q \\ &\qquad lhfle, lhfln \;\;\;\leftarrow \text{ compute vertical integral of atmospheric latent heat flux using } \vec{v}, q, T_c \\ &\qquad tefle, tefln \;\;\;\;\leftarrow \text{ compute vertical integral of atmospheric moist static plus kinetic energy fluxes using } \vec{v}, q, T_c, \Phi_S \\ &\qquad wvfle, wvfln \leftarrow \text{ compute vertical integral of atmospheric water vapour flux using } \vec{v}, q \\ &\qquad lhdiv \;\;\leftarrow \text{ compute divergence of vertical integral of atmospheric latent heat flux using } lhfle, lhfln \\ &\qquad tediv \;\;\leftarrow \text{ compute divergence of vertical integral of atmospheric moist static plus kinetic energy flux using } tefle, tefln \\ &\qquad wvdiv \leftarrow \text{ compute divergence of vertical integral of atmospheric water vapour flux using } wvfle, wvfln \\ &\text{end do} \end{align} \)

Validation

The divergence fields in this dataset exhibit zero global mean suggesting  optimal computations and good accuracy. Tendency terms are temporally stable and exhibit long-term global zero mean indicating good reliability.  Indirectly estimated oceanic F_S derived from tediv and tetend in combination with F_TOA from CERES-EBAF (not in this dataset) agrees with the observation-based ocean heat uptake to within 1 W m^-2 (see Mayer et al. 2022).  All fields are in good qualitative agreement with known patterns of the respective quantities, but satisfaction of physical constraints (e.g., magnitude of ocean-to-land energy and moisture transport or temporal stability) is much improved compared to earlier evaluations (see Mayer et al. 2021 and 2022 for comprehensive evaluation). 

Known issues

1. The divergence terms (tediv, lhdiv, wvdiv) with full spectral resolution show artificial pattern of numerical noise over high topography, which are thus spectrally truncated at wave number 180. The divergence fields with full spectral resolution (see example in Fig. 1) can be reconstructed by computing the divergence of corresponding north- and eastward fluxes provided in this dataset.
2. The ocean-to-land energy transport as estimated from tediv exhibits an unrealistically strong gradual change in the late 1990s and early 2000s, which likely stems from changes in the observing system that has been assimilated by ERA5 (see Mayer et al. 2021 for discussion).
3. Global ocean and land averages of wvdiv exhibit a reasonably strong but statistically insignificant trend over the available period, see Mayer et al. (2021) for further details. 

Figure 1: The divergence of vertical integral of atmospheric moist static plus kinetic energy flux (left) truncated at wave number 180, and (right) with full spectral resolution.

Licence, Acknowledgement and Citation

This dataset is provided under the licence to use Copernicus Products.

All users of this dataset must:

• acknowledge according to the licence to use Copernicus Products
• provide clear and visible attribution to the Copernicus programme by citing the web Climate Data Store (CDS) catalogue entry as follows:

Mayer, J., Mayer, M., Haimberger, L.,(2022): Atmospheric energy and moisture budget data from 1979 to present derived from ERA5 reanalysis, [specify version used e.g. v1.0], Copernicus Climate Change Service (C3S) Climate Data Store (CDS). (Accessed on <DD-MMM-YYYY>), <location i.e. doi/url TBC>.

Please refer to How to acknowledge and cite a Climate Data Store (CDS) catalogue entry and the data published as part of it for complete details.

The authors of this dataset are financially supported by the Austrian Science Funds project P33177. The dataset is created as in-kind contribution to Copernicus. 

References

Mayer, J., Mayer, M. and Haimberger, L., (2022). Comparison of Surface Energy Fluxes from Global to Local Scale. Accepted in Journal of Climate (DOI not assigned yet).

Mayer, J., Mayer, M. and Haimberger, L., (2021). Consistency and Homogeneity of Atmospheric Energy, Moisture, and Mass Budgets in ERA5. Journal of Climate 34(10), 3955-3974. https://doi.org/10.1175/JCLI-D-20-0676.1

Mayer, M., Haimberger, L., Edwards, J. M., and Hyder, P. (2017). Toward consistent diagnostics of the coupled atmosphere and ocean energy budgets. Journal of Climate, 30(22), 9225-9246. https://doi.org/10.1175/JCLI-D-17-0137.1

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