4.6 Hot Topics Genesis Scale Interactions Relationship to Tropical Cyclogenesis

4.6.1 On the Genesis of African easterly waves (1) Two theories for the Genesis of AEWs (2) Idealised Modeling Results (3) Conclusions and Perspectives Chris Thorncroft, Nick Hall and George Kiladis

I: AEWs are generated via a linear mixed barotropic-baroclinic instability mechanism (1) Two Theories for the Genesis of AEWs 925hPa  315K PV AEJ satisfies the necessary conditions for barotropic and baroclinic instability: Burpee (1972), Albignat and Reed, 1980). Therefore we expect AEWs to arise from small random perturbations consistent with a “survival of the fittest” view. Continues to be the consensus view.

I: AEWs are generated via a linear mixed barotropic-baroclinic instability mechanism (evidence against!) (1) Two Theories for the Genesis of AEWs The AEJ is too short! The jet is typically o long. It can only support two waves at one time. It is therefore not possible for AEWs to develop via a linear instability mechanism. The AEJ is only marginally unstable! Hall et al (2006) showed that in the presence of realistic boundary-layer damping the AEW growth rates are very small or zero. It is therefore not possible for AEWs to develop sufficiently fast to be important.

I: AEWs are generated via a linear mixed barotropic-baroclinic instability mechanism (evidence against!) (1) Two Theories for the Genesis of AEWs The AEJ is too short! The jet is typically o long. It can only support two waves at one time. It is therefore not possible for AEWs to develop via a linear instability mechanism. The AEJ is only marginally unstable! Hall et al (2006) showed that in the presence of realistic boundary-layer damping the AEW growth rates are very small. It is therefore not possible for AEWs to develop sufficiently fast to be important. So what can account for the existence of AEWs, their genesis and intermittancy?

(1) Two Theories for the Genesis of AEWs II: AEWs are generated by finite amplitude forcing upstream of the region of observed AEW growth. Carlson (1969) suggested the importance of convection and upstream topography for the initiation of AEWs. Others pushed the linear instability hypothesis. More recent observational evidence has been provided by: Berry and Thorncroft (2005): case study of an intense AEW Kiladis et al (2006):composite analysis Mekonnen et al (2006):climatological view

(2) Idealised Modeling Results More observational and modeling studies are required to explore the validity of the hypothesis that AEWs triggered by upstream forcing. Here we use an idealised modeling study (following Hall et al, 2006): Global spectral primitive equation model Resolution: T31 and 10 levels in the vertical Low-level damping is included (AEWs are stable!) Basic state is fixed.

(2) Idealised Modeling Results Basic state is the observed JJAS mean flow from NCEP ( )

(2) Idealised Modeling Results Most unstable normal mode for the observed zonally varying basic state (Hall et al, 2006). Structure compares well with previous composites based on observations including Kiladis et al (2006). Due to damping this normal mode structure is stable! So why do we observe AEWs? Perturbation streamfunction at sigma=0.850 (top) and in cross section through 15N. Dark shading is ascent, light shading is descent.

(2) Idealised Modeling Results We hypothesize that observed AEWs are triggered by upstream heating due to convection. To explore this hypothesis we apply heating in the jet entrance for one day and consider the adiabatic response to this. This heating is meant to represent the integrated effect of several MCSs. The half width of the circular heating is about 140km. Heating rate profiles (K/day) as a function of sigma. Stratiform Deep Shallow

(2) Idealised Modeling Results Basic state is the observed JJAS mean flow from NCEP ( ) X Initial heating located at (15N, 20E)

(2) Idealised Modeling Results Deep Heating Run

(2) Idealised Modeling Results Shallow Heating Run

(2) Idealised Modeling Results Stratiform Heating Run

(2) Idealised Modeling Results

Summary of heating runs: In all runs the atmospheric response to the heating takes the form of enhanced and coherent AEW-activity in the downstream AEJ. While the subsequent forced normal mode structure appears to be insensitive to the initial heating profile, the amplitude clearly is. A heating profile that creates more intense lower tropospheric circulations (closer to the AEJ) results in larger amplitudes at day 1and after this. The timing of the trough passage at 10W is also sensitive to the heating profile.

(2) Idealised Modeling Results Summary of heating runs: In all runs the atmospheric response to the heating takes the form of enhanced and coherent AEW-activity in the downstream AEJ. While the subsequent forced normal mode structure appears to be insensitive to the initial heating profile, the amplitude clearly is. A heating profile that creates more intense lower tropospheric circulations (closer to the AEJ) results in larger amplitudes at day 1and after this. The timing of the trough passage at 10W is also sensitive to the heating profile. So where is the best place to trigger AEWs?

(2) Idealised Modeling Results Influence function for each profile defined by the root mean square streamfunction at sigma=0.85 and day 10. Confirms greater efficency of shallow and stratiform heating profiles compared to the deep heating profile. Best location to trigger an AEW is around 20N, 15E: close to AEJ entrance and slightly north of basic runs.

(3) Conclusions and Perspectives Significance for weather prediction A significant convective outbreak in the Darfur region will favor the formation of a train of AEWs to the west over sub-Saharan Africa within a few days. For daily-to-medium range forecasts of AEWs, it is important to monitor, and ultimately predict, the nature of the upstream convection.

(3) Conclusions and Perspectives Significance for longer timescales In addition to considering the nature of mean AEJ, we should consider the nature and variability of finite amplitude convective heating precursors.

(3) Conclusions and Perspectives Future work To address issues that relate to variability and predictability of AEWs including their intermittency we should consider: the nature of upstream finite amplitude heating triggers how the heating interacts with the wave itself. how the nature of the observed AEJ impacts the response to these triggers and to the convection within the waves.

4.6.2 Scale Interactions Studies like Reed et al (1977) and Kiladis et al (2006) highlight the typical observed relationship between the AEW dynamical fields and the convection (and associated rainfall). They do not directlly address how AEWs interact with convection.

4.6.2 Scale Interactions The PV-Theta thinking framework is ideal to explore these scale interactions. To introduce this – the following slides show some results from Berry and Thorncroft (2005):

Selection of case. Chose the most intense AEW of summer 2000 from 700hPa meridional wind hovmoller. Case chosen was later associated with Hurricane Alberto. 700hPa Meridional (v) wind, averaged 5 o N-15 o N. (+ve values contoured, >+2ms -1 shaded) Case Study of an intense African easterly wave

Mean State. Mean 700hPa U wind, 16 th July – 15 th August 2000

Mean State: 16 th July – 15 th August hPa  315K PV Strong baroclinic zone 10 o - 20 o N PV ‘strip’ present on the cyclonic shear side of AEJ. 925hPa  e High  e strip exists near 15 o N Mean State supports Baroclinic waves and MCSs!

Satellite imagery METEOSAT-7 Water Vapour channel. Shown every 6 hours from 30 th July z to 4 th August z.

1 st August 00z ((((())))) 700hPa Meridional wind (shaded, ms -1 ), 850hPa Relative Vorticity (contoured x10 -5 s -1 )

1 st August 12z ((((())))) 700hPa Meridional wind (shaded, ms -1 ), 850hPa Relative Vorticity (contoured x10 -5 s -1 )

2 nd August 00z ((((())))) 700hPa Meridional wind (shaded, ms -1 ), 850hPa Relative Vorticity (contoured x10 -5 s -1 )

2 nd August 12z ((((())))) 700hPa Meridional wind (shaded, ms -1 ), 850hPa Relative Vorticity (contoured x10 -5 s -1 )

((((())))) 700hPa Meridional wind (shaded, ms -1 ), 850hPa Relative Vorticity (contoured x10 -5 s -1 ) 3 rd August 00z

3 rd August 12z ((((())))) 700hPa Meridional wind (shaded, ms -1 ), 850hPa Relative Vorticity (contoured x10 -5 s -1 )

PV-theta analysis of AEWs PV-theta highlight synoptic scales and structures associated with baroclinic growth (adiabatic) PV is generated in regions of moist convection; in particular in the vicinity of MCSs (diabatic)

315K (~650hPa) PV (Shaded), 925hPa  anomaly (contour), 925hPa Wind vectors. 1/8/00 00UTC (((((((()))))))) PV structure very different to mean – meandering strip with embedded PV maxima.

1/8/00 12UTC (((((()))))) 315K (~650hPa) PV (Shaded), 925hPa  anomaly (contour), 925hPa Wind vectors. System retains baroclinic growth configuration, PV maxima intensified by convection, 925hPa cyclonic flow strengthens.

2/8/00 00UTC (((((())))))) 315K (~650hPa) PV (Shaded), 925hPa  anomaly (contour), 925hPa Wind vectors. 7K  anomaly, with strong (nearly 20ms -1 ) 925hPa circulation. PV generated over Guinea highlands.

2/8/00 12UTC ((((((((())))))))) 315K (~650hPa) PV (Shaded), 925hPa  anomaly (contour), 925hPa Wind vectors. Disintegration of baroclinic structure. Interaction between system PV and Guinea Highlands PV.

3/8/00 00UTC (((((((()))))))) 315K (~650hPa) PV (Shaded), 925hPa  anomaly (contour), 925hPa Wind vectors. Merger of PV maxima establishes a 925hPa circulation.  anomaly moves to North and West.

3/8/00 12UTC ((((())))) 315K (~650hPa) PV (Shaded), 925hPa  anomaly (contour), 925hPa Wind vectors. Further development of PV maxima gives a strong vortex with significant circulation at 925hPa (22ms -1 on East side).

A conceptual model for AEW life-cycles Phase I: Initiation Phase II: Baroclinic growth Phase III: West coast developments

 ’ Max Conceptual framework (i) Initiation. In the Alberto case a large MCS or several MCSs provides an initial disturbance on a basic state that supports AEWs. Initial value problem?

 ’ Max 700hPa Trough Conceptual framework (ii) Baroclinic growth.

 ’ Max 700hPa Trough Conceptual framework (ii) Baroclinic growth.

 ’ Max 700hPa Trough

Conceptual framework (iii) Merger of PV maxima.

PV-theta analysis of AEWs PV-theta highlight synoptic scales and structures associated with baroclinic growth (adiabatic) PV is generated in regions of moist convection; in particular in the vicinity of MCSs (diabatic)

PV-theta analysis of AEWs PV-theta highlight synoptic scales and structures associated with baroclinic growth (adiabatic) PV is generated in regions of moist convection; in particular in the vicinity of MCSs (diabatic) To complete the analysis we need also to understand what aspects of the AEW encourage or discourage convection.

PV-theta analysis of AEWs – How do AEWs favour convection? Adiabatic forcing of ascent? Destabilzation and reduced CIN? Recent modeling results (Berry, 2008) favour the latter. CIN decreases steadily between the northerlies and the trough – convection gets triggered before the trough though. But there may be strong case-to-case variability.

PV-theta analysis of AEWs – What is needed for growth? Need +ve PV anomalies to be located where the AEW trough is. If they occur ahead they will only affect propagation (cf Diabatic Rossby Waves – Parker and Thorpe (1995) If they occur in the ridge then they will result in decay of the AEW.

PV-theta analysis of AEWs – Scale Interactions Synoptic-Mesoscale Interactions

PV-theta analysis of AEWs – Scale Interactions Synoptic-Mesoscale Interactions From a PV-theta perspective, the heating rate profiles are crucial to know and understand.

PV-theta analysis of AEWs – Scale Interactions Synoptic-Mesoscale Interactions From a PV-theta perspective, the heating rate profiles are crucial to know and understand. Mesoscale-Microscale Interactions Ultimately these profiles are influenced by the nature of the microphysics!

4.6.3 Relationship to Tropical Cyclogenesis USA West Africa

Atlantic Tropical Cyclone Variability (ATCV) There exists marked interannual to decadal variability in ATCV. What are the causes? Are they predictable?

Atlantic Tropical Cyclone Variability (ATCV) Known factors: Tropical Atlantic SSTs ENSO West African rainfall Phase of QBO!!!

Atlantic Tropical Cyclone Variability (ATCV) Known factors: Tropical Atlantic SSTs ENSO West African rainfall Phase of QBO!!!

Atlantic Tropical Cyclone Variability (ATCV) Goldenberg and Shapiro (1996) Linear correlation coefficients: ENSO – ATCV Sahel Rainfall – ATCV+0.70 Why is West Africa so important? large-scale environmental impacts (e.g. shear) weather systems (possibly)

Atlantic Tropical Cyclone Variability vertical wind shear between 200mb and 925mb

Atlantic Tropical Cyclone Variability Understanding the processes that influence the MDR shear and its variability is very important West Africa and East Pacific both provide important anomalous heat sources that can impact the MDR shear through tropical teleconnections

Atlantic Tropical Cyclone Variability Thorncroft and Hodges (2001) What about variability in the weather systems?

Atlantic Tropical Cyclone Variability There is a hint that the number of strong vortices leaving the West African coast impacts ATCV but this is far from being a sure case. Recent analysis in the ERA40 datset (Hopsch et al, 2006) suggests this relationship to be weak on interannual timescales - but not on interdecadal timescales!

West Coast Developments Case Studies have indicated that there can be significant enhancement of the circulations, including at low-levels, just before the AEWs leave the African coast. BIG question: Do AEWS matter? Composite analysis from Hopsch (2008) shows some recent results relevant to this question.

Composite for developing AEWs: PV at 600hPa streamfunction of 2-6 day filtered wind

Composite for non-developing AEWs: PV at 600hPa streamfunction of 2-6 day filtered wind

Cross section for coast storm AEWs (i.e. storms forming east of 30°W) all cross-sections are along 40°W-10°E at 11.25°N black arrow points to composite trough location

Shaded: VOR (Red = pos, Blue = neg) Horizontal Wind at all levels Theta-e Shaded: RH (Red < 50% Blue > 60%) Vertical wind Day -2

Day -1

Day 0

Day +1

Day +2

Cross section for non-developing AEWs

Day -2

Day -1

Day 0

Day +1

Day +2

4.7 Easterly waves in other tropical regions

Builds on Schubert et al 1991 “Potential Vorticity modeling of the ITCZ and the Hadley circulation JAS, 48, Consider PV sign-reversals associated with “ITCZ-convection”

4.7 Easterly waves in other tropical regions

ITCZ breaks down in association with barotropic instability

4.7 Easterly waves in other tropical regions

4.8 Final Comments Easterly waves are present everywhere in the tropics They are particularly important over West Africa where they grow through baroclinic and barotropic energy conversions. The baroclinic energy conversions are particularly strong consistent with the strong baroclinic zone – not present in other tropical regions. AEWs are likely forced by upstream heating associated with convection. AEWs grow through interaction of Rossby waves (adiabatic) and are enhanced by convection (Extra PV-sources) – although we can expect marked case-to-case variability. Hot Research Topics: Genesis Scale Interactions Variability (especially intraseasonal-to-interannual) Relationship to Tropical Cyclones

4.8 Final Comments Easterly waves are also studied in the Caribbean and Pacific where they are often linked to tropical cyclogenesis Some questions: To what extent are the EWs generated in situ or come from upstream (e.g. West Africa)? What can explain the observed phase relationships – why do they vary between Africa and the ocean? How do they interact with equatorial waves?