# Representation of Ethiopian Wet Spells in Global and Nested Models

Authors: Mark R. Jury; Sen Chiao
Journal: Advances in Meteorology
 (2014)

---

## Abstract

Weather forecast and reanalysis models exhibit different performance in daily rainfall estimation over the Ethiopian highlands, 2000–2012, with ECMWF closer to observations than other models. Background is given to illustrate the Hadley circulation and easterly jets over Ethiopia, using sections on 37°E in July–August 2011. ECMWF reanalysis has a narrow band of rainfall >15 mm/day on 10°N, consistent with TRMM satellite estimates, associated with a steep gradient in meridional wind. MERRA and GFS models have a wider band of rainfall and weaker gradients in meridional winds. The contrasting background states influence a nested WRF model simulation of heavy rain in the upper Nile Valley on 29 July, 2011. The GFS (ECMWF) initialization yields stronger northerly (southerly) winds north (south) of Ethiopia, while aircraft observations are southerly at 850 mb and northerly at 700 mb. ECMWF produces heavy and widespread rainfall consistent with observations, with a potentially more realistic simulation of the Hadley circulation.


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## Body

## 1. Introduction

Recent floods across Africa have restored water resources and improved crop yields, but also disrupted millions of lives [1–3]. Seasonal runoff ~50
·
10
9 m3/yr from the Ethiopian highlands sustains the Nile River [4–9] and tends to peak in August with a northerly shift of the equatorial trough and meridional Hadley circulation. An easterly jet induced by Indian monsoon outflow spreads convection across the Sahel [10–14] depending on links between the Atlantic Walker circulation and Pacific Ocean heat anomalies [15–17].National meteorological agencies tasked with short-term weather forecasts often use a nested mesoscale model such as Weather Research and Forecasting (WRF, [18]). However, model sensitivity to global initialization data and parameterization options [19, 20] are often untested, so forecasters must uncover bias in successive operational applications. To improve guidance, this research evaluates global and nested model ability to represent the Ethiopian atmospheric circulation, thermodynamic conditions, and convection during wet spells. Key features for consideration include the influx of tropical moisture, subtropical subsidence and heating, orographic and diurnal forcing, the thermal easterly jets, gradients in the meridional circulation, and rainfall intensity and location. In Section 2 the data and methods are outlined. Section 3 compares global model rainfall and its forcing in July–August, 2011, over northeast Africa and then focuses on a wet spell over the Ethiopian highlands. Nested model outcomes with two contrasting initialization schemes are evaluated, and conclusions are given in Section 4.


## 2. Data and Methods

Observational products used in this study include hourly 0.2° Coupled Forecast System (CFS, [21]) NOAH-parameterized [22] data, 3-hourly 0.25° cMorph multisatellite estimates [23], daily 0.1° African Rainfall Climatology observations (ARC2, [24]), monthly 0.5° gauge observations interpolated by the Global Precipitation Climatology Center (GPCC, [25]), and monthly 0.5° satellite estimates from the Tropical Rainfall Monitoring Mission (TRMM). Our focus is a longitude slice and grid-cell in the Nile River catchment (Figure 1(a)). Ethiopian rainfall from various sources has been evaluated by Verdin et al. [26], Dinku et al. [27], and Jacob et al. [28]. Background data on surface temperature and vegetation fraction were analyzed from 1 km MODIS satellite [29]. Hourly surface evaporation and runoff were analyzed from the Global Land Data Assimilation System GLDAS [30].(a) MODIS land surface temperature 15 July–15 August, 2011, and elevation contours at 800 m intervals. (b) July–August, 2011, N-S section on 37°E of the circulation (meridional vertical VW vectors, max = 5 m/s), zonal wind (shaded), relative humidity >70% (contours), and temperature >25°C (dashed) from NCEP2, with topographic profile. (c) Intercomparison of cross-correlations between model estimated daily rainfall and ARC2 observations 2000–2012, for a 1° grid-cell (dashed in a), in diminishing seasons.
(a)
(b)
(c)The model fields for consideration are 3-hourly and daily 1° Global Forecast System (GFS) analyses, 1° European Community Medium-range Weather Forecasts interim reanalysis (ECMWF, [31]), 1° NASA Modern Reanalysis (MERRA, [32, 33]), monthly 2° National Center for Environmental Prediction reanalysis (NCEP2, [34]), and 2° Climate Data Assimilation System (CDAS1) analyses. The variables employed are meridional and zonal winds at 850–200 mb levels, vertical motion, relative humidity, surface skin and air temperature, latent heat flux, and evaporation and surface runoff. Runoff from the Ethiopia highlands has been studied [35, 36]; here, an area-average is considered.The methodology used to evaluate model outputs progresses from broad to narrow, first considering July–August, 2000–2012, averages representative of mid-summer. Data are analyzed on a meridional section at 37°E ± 1° from 5°S–30°N (northeast Africa). Cross-correlations between model daily rainfall and observations are calculated over the highlands and for a Nile Valley grid-cell (11°N, 37°E) in the period 2000–2012. The sample size is progressively reduced from all-year (N
=
4748) to wet months (N
=
806) to focus on model ability to represent daily rainfall timing and intensity. The erratic nature of rainfall provides ~70 degrees of freedom for continuous records and ~250 for wet months, so correlations > 0.1 are significant at 90% confidence. Next, weather conditions in the Ethiopian highlands on 29 July, 2011, are analyzed from global fields and aircraft meteorological data relay (AMDAR) profiles. Twenty-four hour ensemble back-trajectories are calculated by the Hysplit model for an end-point at 11°N, 37°E, 1000, and 3000 m above ground using GFS data. Lastly mesoscale model simulations are compared with Meteosat cloud top temperatures.Nested model simulations of rainfall, radar reflectivity, and winds are performed using the nonhydrostatic WRF version 3.2.1. The model is configured with a horizontal grid of 3 km over the Ethiopian highlands; it has 90 vertical sigma levels from surface to 10 mb. The WRF options used are Lin microphysics, NOAH surface scheme, MYJ planetary boundary layer, BMJ cumulus parameterization, and RRTM atmospheric radiation. A 36-hr simulation is conducted starting at 00:00 LST 29 July, 2011, to capture a full diurnal cycle. Two distinct runs are made: in the first the initial and time-dependent lateral boundary conditions are derived from GFS and in the second they are derived from ECMWF. Outputs at the time of peak rainfall (18:00–24:00 LST) are considered.


## 3. Results

### 3.1. Background and Seasonal Features

The Ethiopian highlands are cool during summer with land surface temperatures <20°C at elevations above 1600 m (Figure1(a)). West of the escarpment at 39°E AIRS satellite-derived clouds exceed 50% coverage in July–August, 2011. In the surrounding lowlands, day-time land surface temperatures exceed 50°C and heat fluxes lift the boundary layer >1 km. The diurnal heating pattern resembles a warm ring surrounding a 5
°
×
5
° cool center; consequently, highland thunderstorms build towards sunset.Key features of the large-scale seasonal environment in July–August, 2011, are illustrated in Figure1(b) by N-S section on 37°E. Easterly jets are seen in the 600 mb and 150 mb layers over the northern highlands 8–16°N. Relative humidity exceeds 80% in a dome up to 500 mb over the southern highlands 4–12°N, according to NCEP2 data. A warm surface layer >25°C in the latitudes 16–30°N lies beneath the northern Hadley circulation that tilts over the northern highlands. The southern Hadley circulation is reflected in meridional overturning above the Turkana Valley (2–4°N). The two Hadley cells create deep ascent over Ethiopia that is enhanced by cyclonic vorticity near the easterly jets (Figure 1(b)).Our aim here is to evaluate model simulated rainfall over the highlands. In Figure1(c) daily analyses for the 11°N, 37°E grid-cell are cross-correlated with ARC2 observations in the period 2000–2012. Considering the whole year, models achieve significant cross-correlations (>0.35) and thus capture the annual cycle, the dry season, and minor rain events. Standard deviations are ARC2 4.8 mm/day, GPCC 5.9, GFS 7.8, and ECMWF 11.3. As the season is narrowed, eliminating the annual cycle and no-rain days, the correlations decline (as degrees of freedom increases). With a July–August window, the ECMWF reanalysis obtains a daily cross-correlation > 0.1 (Figure 1(c)), while GFS, MERRA, and CDAS1 are near zero. These findings are consistent with Bosilovich et al. [37], wherein the Taylor diagram of African seasonal rainfall puts ECMWF closer to observation than other reanalyses. This raises three questions. Why do the global models perform differently? Are discrepancies due to assimilation or parameterization? How will the performance of nested mesoscale models be affected by initialization source? The answers to these questions could improve short-range flood forecasts.To understand why models produce different local rainfall, comparisons are made along the 37°E longitude slice averaged for July–August 2000–2012. This macro perspective is useful to diagnose key features in MERRA and ECMWF outputs [38]. The models exhibit similarities in 850 mb meridional winds and 500 mb zonal winds (not shown). Significant differences are found in the upper meridional winds and rainfall (Figures 2(a), 2(b), and 2(d)). The ECMWF model has a sharper d
V
200
/
d
y gradient with min/max at 6°N/15°N, while the MERRA model has a weaker gradient and min/max at 2°N/18°N. The weaker gradient coincides with a broader band of seasonal rain in MERRA with peaks on 0°N, 9°N, and 13°N in accord with GPCC observations. In contrast, ECMWF simulates a single zone of heavy rain at 10°N that is close to TRMM estimates (cf. [39]). Latent heat fluxes also show differences (Figure 2(c)), with MERRA transpiration double ECMWF over the highlands. Yet both exhibit a U-shape suggesting that winds penetrate the edges but not the densely vegetated interior (9°N). The two models have similar latent heat fluxes over the Red Sea (23-24°N) and exhibit a high/low pattern over the equator/Turkana Valley. The feedback between surface transpiration and convection is known to affect model performance [40].Mean July–August, 2000–2012, variables along N-S slice on 37°E for ECMWF and MERRA models: (a) 200 mb meridional wind, (b, d) rainfall from model and GPCC/TRMM observations, and (c) model latent heat flux.
(a)
(b)
(c)
(d)


### 3.2. Wet Spell Characteristics

Given our interest in short-term flood forecasts, attention is turned to a case of heavy rainfall in the last week of July 2011. Time series of CFS rainfall and GLDAS evaporation and runoff are given in Figure3(a) for the 11°N, 37°E grid-cell. Evaporation followed the diurnal cycle of solar radiation peaking at ~16 mm/day, while rainfall fluctuated up to ~40 mm/day around sunset (cf. [41, 42]). GLDAS runoff was <10% of rainfall (cf. [43, 44]) and was highest on the 29th. The map of CFS rainfall on 29 July, 2011, (Figure 3(b)) reveals widespread values >5 mm and isolated areas >50 mm between 10–13°N and 36–38°E. This wet spell spawned a number of squall lines that moved westward across the Sahel, causing heavy rains at N’Djamena and eventually consolidating off Dakar into an African easterly wave that passed through the Caribbean.(a) CFS rainfall, evaporation, and runoff hourly time series for 1° grid-cell centered on 11°N, 37°E in the period 26 July–2 August, 2011. (b) CFS mean rainfall map (mm/day) on 29 July with urban centers.
(a)
(b)A synoptic weather analysis for 29 July, 2011, is provided in Figure4. The GFS and ECMWF models are consistent in their representation of surface temperature. A tongue of cold air extends along 38°E (Figure 4(a)) where elevation exceeds 2000 m. The GFS 500 mb winds were easterly >10 m/s north of 10°N (Figure 4(b)). GFS 850 mb relative humidity exhibited a gradient between a dry cell in the northeast and a moist zone in the southwest (Figure 4(c)). 850 mb winds were south-westerly over Sudan, rotated to north-westerly over Eritrea and in the dry zone, and wrapped into a vortex at 11°N, 39°E.Regional weather features on 29 July, 2011: (a) surface air temperature (GFS contoured, ECMWF shaded), (b) GFS 500 mb wind (speed shaded), and (c) GFS 850 mb relative humidity (shaded), and 850 mb wind vectors (max = 12 m/s) and streamlines.
(a)
(b)
(c)Three AMDAR aircraft profiles (Figure5) highlight wind shear on the evening of 29 July, 2011. Winds below 3200 m (~700 mb) were light (5 m/s) and from the south-west at Addis Ababa and from north-west at Asmera. There was a weak temperature inversion at 3000 m (725 mb) at Asmera, above which winds rotated to easterly. An easterly jet of 15 m/s was observed in the 5000–6000 m layer (~500 mb) in all three profiles. A key feature of the AMDAR profiles at Addis Ababa was the prevalence of surface layer south-westerly flow and an absence of northerly winds. The temperature lapse rate was −6.8°C/km and thus conditionally unstable.AMDAR aircraft wind profiles for evening of 29 July, 2011 (height—m, speed—m/s).
(a)
(b)
(c)
(d)
(e)
(f)Twenty-four hour back-trajectories for an endpoint at 11°N, 37°E, 1000 m, and 3000 m above ground are illustrated in Figures6(a) and 6(c) in plan and section view. The 3000 m ensemble trajectories (based on GFS data) converged from Eritrea between the Red Sea (SST ~30°C) and Lake Tana (25°C) and exhibited a rising component. Along-path relative humidity increased from 62% to 85%. The 1000 m ensemble trajectories converged from the southwest where the underlying vegetation fraction exceeds 0.5 (Figure 6(b)). Back-trajectories at both levels exhibited clockwise, anticyclonic curvature. The GFS meteogram for the grid-cell (Figure 6(d)) highlights diurnal fluctuations: winds increased in the evening, following peaks in the boundary layer height (700 m at 12:00) and convective available potential energy (2000 J/kg at 15:00). The diurnal peak of rainfall was 18:00–24:00 LST, totaling ~30 mm. A key finding is that the GFS model emphasizes the surface northerly winds observed at Asmera.24 hr ensemble back trajectories ending at 11°N, 37°E at 22:00 LST 29 July, 2011: (a) for 3000 m above ground with SST, (b) MODIS vegetation fraction during the period, (c) trajectories ending 1000 m above ground, and (d) GFS meteogram of winds, PBL height, CAPE, and rainfall at 3-hr intervals at 11°N, 37°E. Map scales vary; GFS relative humidity along (vertical section) path is given in (a, c).
(a)
(b)
(c)
(d)


### 3.3. WRF Model Simulation

The WRF model simulation of the 29 July, 2011, convective outbreak, with contrasting GFS and ECMWF initialization, is presented in Figures7(a)–7(f). It offers a snapshot assessment of how the two models handled afternoon to evening thunderstorm development. The ECMWF-WRF simulated radar reflectivity was widespread in the north, while winds were easterly to the east and southerly to the south. The GFS-WRF simulation located the thunderstorms further south in response to stronger northerly flow at 700 mb. The thunderstorms aggregated more in the ECMWF-WRF simulation, while the GFS-WRF simulation had isolated cells, for example, 10-11°N, 36-37°E.High resolution WRF simulated radar reflectivity and 700 mb wind with GFS initialization (left) and ECMWF (right) for 29 July, 2011: (a) 20:00 LST, (b) 22:00 LST, and (c) 24:00 LST.
(a)
(b)
(c)A vertical NE-SW section analysis of these simulations (Figures8(a)–8(d)) reveals weaker convection in the GFS-WRF run associated with northerly flow over the northern highlands (V < −8 m/s at 3 km). While the ECMWF-WRF simulation spread convection into the Nile Valley, the GFS-WRF estimated radar reflectivity was more isolated. The ECMWF-WRF run had southerly flow over the southern highlands (V > +8 m/s to 5 km). Hence, the WRF simulation reveals a stronger southern (northern) Hadley cell when initialized with ECMWF (GFS) data in this case. Together with the earlier seasonal analysis of meridional winds (cf. Figure 2(a)), there is a reason why the ECMWF better represents the timing and intensity of daily rainfall.High resolution WRF simulated vertical NE-SW section (cf. Figure9(a)) of meridional (V) wind (contour interval 2 m/s, dashed southward) and radar reflectivity (shaded according to scale upper right) at (a) 20:00 LST and (b) 22:00 LST; initialization with GFS (left) and ECMWF (right). Arrows highlight contrasting meridional flow.
(a)
(b)
(c)
(d)Rainfall maps at 18:00, 20:00, and 22:00 LST from the two simulations are given in Figures9(a) and 9(b) in comparison with Meteosat cloud top temperatures (Figure 9(c)). The GFS-WRF simulation had westward propagating cells that separated into two meridional squall lines. The ECMWF-WRF simulation had rainfall further north in meridional bands that aggregated with time, in qualitative agreement with the Meteosat images. While this case has highlighted key differences, a greater sample of nested runs would be needed to make a conclusive argument.WRF simulated rainfall on 29 July for (a) 18:00, (b) 20:00, and (c) 22:00 LST, with max shading = 75 mm/day. GFS initialization (left), ECMWF (middle), and comparison with Meteosat IR images (right). Red dashed line in (a, left) is Figure8 section.
(a)
(b)
(c)


## 3.1. Background and Seasonal Features

The Ethiopian highlands are cool during summer with land surface temperatures <20°C at elevations above 1600 m (Figure1(a)). West of the escarpment at 39°E AIRS satellite-derived clouds exceed 50% coverage in July–August, 2011. In the surrounding lowlands, day-time land surface temperatures exceed 50°C and heat fluxes lift the boundary layer >1 km. The diurnal heating pattern resembles a warm ring surrounding a 5
°
×
5
° cool center; consequently, highland thunderstorms build towards sunset.Key features of the large-scale seasonal environment in July–August, 2011, are illustrated in Figure1(b) by N-S section on 37°E. Easterly jets are seen in the 600 mb and 150 mb layers over the northern highlands 8–16°N. Relative humidity exceeds 80% in a dome up to 500 mb over the southern highlands 4–12°N, according to NCEP2 data. A warm surface layer >25°C in the latitudes 16–30°N lies beneath the northern Hadley circulation that tilts over the northern highlands. The southern Hadley circulation is reflected in meridional overturning above the Turkana Valley (2–4°N). The two Hadley cells create deep ascent over Ethiopia that is enhanced by cyclonic vorticity near the easterly jets (Figure 1(b)).Our aim here is to evaluate model simulated rainfall over the highlands. In Figure1(c) daily analyses for the 11°N, 37°E grid-cell are cross-correlated with ARC2 observations in the period 2000–2012. Considering the whole year, models achieve significant cross-correlations (>0.35) and thus capture the annual cycle, the dry season, and minor rain events. Standard deviations are ARC2 4.8 mm/day, GPCC 5.9, GFS 7.8, and ECMWF 11.3. As the season is narrowed, eliminating the annual cycle and no-rain days, the correlations decline (as degrees of freedom increases). With a July–August window, the ECMWF reanalysis obtains a daily cross-correlation > 0.1 (Figure 1(c)), while GFS, MERRA, and CDAS1 are near zero. These findings are consistent with Bosilovich et al. [37], wherein the Taylor diagram of African seasonal rainfall puts ECMWF closer to observation than other reanalyses. This raises three questions. Why do the global models perform differently? Are discrepancies due to assimilation or parameterization? How will the performance of nested mesoscale models be affected by initialization source? The answers to these questions could improve short-range flood forecasts.To understand why models produce different local rainfall, comparisons are made along the 37°E longitude slice averaged for July–August 2000–2012. This macro perspective is useful to diagnose key features in MERRA and ECMWF outputs [38]. The models exhibit similarities in 850 mb meridional winds and 500 mb zonal winds (not shown). Significant differences are found in the upper meridional winds and rainfall (Figures 2(a), 2(b), and 2(d)). The ECMWF model has a sharper d
V
200
/
d
y gradient with min/max at 6°N/15°N, while the MERRA model has a weaker gradient and min/max at 2°N/18°N. The weaker gradient coincides with a broader band of seasonal rain in MERRA with peaks on 0°N, 9°N, and 13°N in accord with GPCC observations. In contrast, ECMWF simulates a single zone of heavy rain at 10°N that is close to TRMM estimates (cf. [39]). Latent heat fluxes also show differences (Figure 2(c)), with MERRA transpiration double ECMWF over the highlands. Yet both exhibit a U-shape suggesting that winds penetrate the edges but not the densely vegetated interior (9°N). The two models have similar latent heat fluxes over the Red Sea (23-24°N) and exhibit a high/low pattern over the equator/Turkana Valley. The feedback between surface transpiration and convection is known to affect model performance [40].Mean July–August, 2000–2012, variables along N-S slice on 37°E for ECMWF and MERRA models: (a) 200 mb meridional wind, (b, d) rainfall from model and GPCC/TRMM observations, and (c) model latent heat flux.
(a)
(b)
(c)
(d)


## 3.2. Wet Spell Characteristics

Given our interest in short-term flood forecasts, attention is turned to a case of heavy rainfall in the last week of July 2011. Time series of CFS rainfall and GLDAS evaporation and runoff are given in Figure3(a) for the 11°N, 37°E grid-cell. Evaporation followed the diurnal cycle of solar radiation peaking at ~16 mm/day, while rainfall fluctuated up to ~40 mm/day around sunset (cf. [41, 42]). GLDAS runoff was <10% of rainfall (cf. [43, 44]) and was highest on the 29th. The map of CFS rainfall on 29 July, 2011, (Figure 3(b)) reveals widespread values >5 mm and isolated areas >50 mm between 10–13°N and 36–38°E. This wet spell spawned a number of squall lines that moved westward across the Sahel, causing heavy rains at N’Djamena and eventually consolidating off Dakar into an African easterly wave that passed through the Caribbean.(a) CFS rainfall, evaporation, and runoff hourly time series for 1° grid-cell centered on 11°N, 37°E in the period 26 July–2 August, 2011. (b) CFS mean rainfall map (mm/day) on 29 July with urban centers.
(a)
(b)A synoptic weather analysis for 29 July, 2011, is provided in Figure4. The GFS and ECMWF models are consistent in their representation of surface temperature. A tongue of cold air extends along 38°E (Figure 4(a)) where elevation exceeds 2000 m. The GFS 500 mb winds were easterly >10 m/s north of 10°N (Figure 4(b)). GFS 850 mb relative humidity exhibited a gradient between a dry cell in the northeast and a moist zone in the southwest (Figure 4(c)). 850 mb winds were south-westerly over Sudan, rotated to north-westerly over Eritrea and in the dry zone, and wrapped into a vortex at 11°N, 39°E.Regional weather features on 29 July, 2011: (a) surface air temperature (GFS contoured, ECMWF shaded), (b) GFS 500 mb wind (speed shaded), and (c) GFS 850 mb relative humidity (shaded), and 850 mb wind vectors (max = 12 m/s) and streamlines.
(a)
(b)
(c)Three AMDAR aircraft profiles (Figure5) highlight wind shear on the evening of 29 July, 2011. Winds below 3200 m (~700 mb) were light (5 m/s) and from the south-west at Addis Ababa and from north-west at Asmera. There was a weak temperature inversion at 3000 m (725 mb) at Asmera, above which winds rotated to easterly. An easterly jet of 15 m/s was observed in the 5000–6000 m layer (~500 mb) in all three profiles. A key feature of the AMDAR profiles at Addis Ababa was the prevalence of surface layer south-westerly flow and an absence of northerly winds. The temperature lapse rate was −6.8°C/km and thus conditionally unstable.AMDAR aircraft wind profiles for evening of 29 July, 2011 (height—m, speed—m/s).
(a)
(b)
(c)
(d)
(e)
(f)Twenty-four hour back-trajectories for an endpoint at 11°N, 37°E, 1000 m, and 3000 m above ground are illustrated in Figures6(a) and 6(c) in plan and section view. The 3000 m ensemble trajectories (based on GFS data) converged from Eritrea between the Red Sea (SST ~30°C) and Lake Tana (25°C) and exhibited a rising component. Along-path relative humidity increased from 62% to 85%. The 1000 m ensemble trajectories converged from the southwest where the underlying vegetation fraction exceeds 0.5 (Figure 6(b)). Back-trajectories at both levels exhibited clockwise, anticyclonic curvature. The GFS meteogram for the grid-cell (Figure 6(d)) highlights diurnal fluctuations: winds increased in the evening, following peaks in the boundary layer height (700 m at 12:00) and convective available potential energy (2000 J/kg at 15:00). The diurnal peak of rainfall was 18:00–24:00 LST, totaling ~30 mm. A key finding is that the GFS model emphasizes the surface northerly winds observed at Asmera.24 hr ensemble back trajectories ending at 11°N, 37°E at 22:00 LST 29 July, 2011: (a) for 3000 m above ground with SST, (b) MODIS vegetation fraction during the period, (c) trajectories ending 1000 m above ground, and (d) GFS meteogram of winds, PBL height, CAPE, and rainfall at 3-hr intervals at 11°N, 37°E. Map scales vary; GFS relative humidity along (vertical section) path is given in (a, c).
(a)
(b)
(c)
(d)


## 3.3. WRF Model Simulation

The WRF model simulation of the 29 July, 2011, convective outbreak, with contrasting GFS and ECMWF initialization, is presented in Figures7(a)–7(f). It offers a snapshot assessment of how the two models handled afternoon to evening thunderstorm development. The ECMWF-WRF simulated radar reflectivity was widespread in the north, while winds were easterly to the east and southerly to the south. The GFS-WRF simulation located the thunderstorms further south in response to stronger northerly flow at 700 mb. The thunderstorms aggregated more in the ECMWF-WRF simulation, while the GFS-WRF simulation had isolated cells, for example, 10-11°N, 36-37°E.High resolution WRF simulated radar reflectivity and 700 mb wind with GFS initialization (left) and ECMWF (right) for 29 July, 2011: (a) 20:00 LST, (b) 22:00 LST, and (c) 24:00 LST.
(a)
(b)
(c)A vertical NE-SW section analysis of these simulations (Figures8(a)–8(d)) reveals weaker convection in the GFS-WRF run associated with northerly flow over the northern highlands (V < −8 m/s at 3 km). While the ECMWF-WRF simulation spread convection into the Nile Valley, the GFS-WRF estimated radar reflectivity was more isolated. The ECMWF-WRF run had southerly flow over the southern highlands (V > +8 m/s to 5 km). Hence, the WRF simulation reveals a stronger southern (northern) Hadley cell when initialized with ECMWF (GFS) data in this case. Together with the earlier seasonal analysis of meridional winds (cf. Figure 2(a)), there is a reason why the ECMWF better represents the timing and intensity of daily rainfall.High resolution WRF simulated vertical NE-SW section (cf. Figure9(a)) of meridional (V) wind (contour interval 2 m/s, dashed southward) and radar reflectivity (shaded according to scale upper right) at (a) 20:00 LST and (b) 22:00 LST; initialization with GFS (left) and ECMWF (right). Arrows highlight contrasting meridional flow.
(a)
(b)
(c)
(d)Rainfall maps at 18:00, 20:00, and 22:00 LST from the two simulations are given in Figures9(a) and 9(b) in comparison with Meteosat cloud top temperatures (Figure 9(c)). The GFS-WRF simulation had westward propagating cells that separated into two meridional squall lines. The ECMWF-WRF simulation had rainfall further north in meridional bands that aggregated with time, in qualitative agreement with the Meteosat images. While this case has highlighted key differences, a greater sample of nested runs would be needed to make a conclusive argument.WRF simulated rainfall on 29 July for (a) 18:00, (b) 20:00, and (c) 22:00 LST, with max shading = 75 mm/day. GFS initialization (left), ECMWF (middle), and comparison with Meteosat IR images (right). Red dashed line in (a, left) is Figure8 section.
(a)
(b)
(c)


## 4. Conclusions

An intercomparison of global model estimates of daily rainfall over the Ethiopian highlands, 2000–2012, determined that ECMWF was closer to ARC2 observations than other models. This was related to the ECMWF representation of seasonal rainfall as a narrow band >15 mm/day on 10°N colocated with a stronger meridional overturning Hadley circulation. The contrasting background states influence a nested WRF model simulation of heavy rains in the upper Nile Valley on 29 July, 2011. The GFS (ECMWF) initialization yields stronger northerly (southerly) 700 mb winds over northern (southern) Ethiopia. AMDAR profiles during the wet spell exhibit south-westerly winds below 700 mb and an easterly jet aloft. The surface inflow passes across the densely vegetated southwestern highlands, suggesting latent heat flux parameterization as a source of contrast that deserves further attention.Back-trajectories moving up from the southwest make a “left hook” around the cool plateau, sweeping across the border of Sudan and Eritrea, before curling into a thunderstorm cluster on 29 July, 2011. Part of the southerly flow over Kenya is entrained into the vortex, but most passes into the Arabian Sea. The stronger southern Hadley penetration onto the Ethiopian highlands by the ECMWF-WRF simulation is suggested to improve its representation of rainfall. The GFS-WRF simulation, in contrast, maintains a stronger northern Hadley circulation that would bring subtropical air to the highlands, inhibiting moist convection.Further progress in mesoscale forecasting of Ethiopian wet spells will depend on better operational access to both local observations and ECMWF initialization fields. The addition of humidity to AMDAR aircraft profiles should contribute to more accurate short-term forecasts. While our case study has highlighted key differences in GFS/ECMWF inputs and WRF model outcomes, a more quantitative assessment of a larger sample of wet spell simulations is needed to better understand Hadley cell interaction with the easterly jets and diurnal convection over the Ethiopian highlands.



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*Source: 237374-2014-03-05.xml*