# Presentation: 627150

## PREDICTION OF FRONTOGENETICALLY FORCED PRECIPITATION BANDS

***P******REDICTION****** ******O******F****** ******F******RONTOGENETICALLY****** ******F******ORCED****** ******P******RECIPITATION****** ******B******ANDS***

**PETER C. BANACOS**
**NWS / Storm Prediction Center**
**WDTB Winter Weather Workshop IV**
**Boulder, CO   ~   23 July 2003**

**Notes:**
Version 7/16 10:00pm. 

## OUTLINE

**Frontogenesis**
- ...where it fits in the forecast process
- kinematics and dynamics of frontogenesis
- synoptic pattern recognition
*Case #1* – examine band formation
**Mesoscale Banding Characteristics**
- modulation by local wind profile
- col point aloft
- modulation by stability
*Case #2* – numerical model considerations

## INGREDIENTS BASED FORECASTING

-  _Purpose_: To focus the forecaster on the necessary conditions (“ingredients”) needed for a specific meteorological event to take place.

*Frontogenesis is a lifting/forcing mechanism. *

## Frontogenesis (definition)

-  The 2-D scalar frontogenesis function (*F* ) – quantifies the change in horizontal (potential) temperature gradient following air parcel motion :
***F  *****> 0 frontogenesis, *****F  *****<  0 frontolysis**
-  Conceptually, the local change in horizontal temperature gradient near an existing front, baroclinic zone, or feature as it moves.

*(S. Petterssen 1936)*

## Vector Frontogenesis Function

*(Keyser et al. 1988, 1992)*

- Change in _magnitude_
-  Corresponds to vertical motion on the frontal scale (mesoscale bands)
- Change in _direction_ (rotation)
-  Corresponds to vertical motion on the scale of the baroclinic wave itself

* ***F** is of fundamental importance...
*	**Galilean invariant*
* **	**full wind generalization of the quasi-geostrophic ****Q****-vector *

## Kinematics of Frontogenesis

-   The geometry of the horizontal flow has a first-order influence on **F** in most situations.
- Examine separate contributions of
- horizontal _divergence_, _deformation_,
- and _vorticity_ to the field of
- frontogenesis.

-  _Note:_   Will focus exclusively on the Petterssen 2-D scalar       	     frontogenesis (Fn)

## Horizontal Divergence

**Horizontal Divergence**

- Divergence (Convergence) acts frontolytically (frontogenetically), always, irrespective of isotherm orientation.

*F*<0

*F*>0

## Horizontal Deformation

- 	Flow fields involving deformation acting frontogenetically are prominent in the majority of banded precipitation cases.

*F*>0

## Horizontal Deformation (cont.)

*F*<0

- Need to consider orientation of isotherms relative to axis of dilatation.

## Vertical Vorticity

**Vertical Vorticity**

- Pure vorticity acts to rotate isotherms, _cannot_ tighten or weaken them.

*F*=0

## Other Contributing Factors to Frontogenesis

- The kinematic field, and deformation in particular, plays the most prominent role in the 2-D frontogenesis aloft.
- Other processes such as diabatic heating and tilting effects may also contribute to frontogenesis.
- _Examples_:
- differential solar heating
- Latent heating with convective motions 			(documented in coastal frontogenesis process).

## Dynamics of Frontogenesis (vertical circulation)

**Dynamics of Frontogenesis ****(vertical circulation)**

- Flow field dominated by deformation.

## Dynamics of Frontogenesis (cont.)

**Dynamics of Frontogenesis (cont.)**

- Ageostrophic circulation develops as a response to increasing temperature gradient.

## Dynamics of Frontogenesis (cont.)

-  When we talk about frontogenesis forcing, it’s the resulting ageostrophic circulation we are most interested in for precipitation forecasting.

**Notes:**
The ageostrophic circulation can become quite strong with time and the eventual response will be an increase in the vertical geostrophic shear, consistent with the thermal-wind equation, at which time the atmosphere would be balanced once again and the secondary circulation would quickly dissipate. Additionally, the slope of the circulation itself is generally back into the colder air (see the Sawyer/Ellisen equation).
It is interesting to note that the same reasoning can be applied to frontolysis forcing, arguing for a thermal indirect circulation with the ascending branch of the circulation located to the cold side of the frontogenesis minimum (i.e. the maximum value in frontolysis). However, because the atmosphere in that case would be attempting to reduce the vertical wind shear, it is possible that much of that could be accomplished through turbulent diffusion of the wind in the vertical. There is no opposite process that could aid in the increase in vertical wind shear, and thus, the robust ageostrophic circulation is a necessary element of frontogenesis forcing but may not be needed in the case of frontolysis forcing. 

## Forecasting Applications

## Use of Frontogenesis in Forecasting

- Presence of *F*  in 850-500mb layer can help diagnose and predict areas of heavy banded precipitation.
- Potential for banding can be assessed using *F* field in numerical models, with placement of banding refined in <12 hour period.
- New graphic forecast tools allow location of banded precipitation to be conveyed to the user.

## Common Synoptic Patterns

**TWO CLASSES OF BANDS:**
- Bands associated with surface cyclogenesis
- Bands not associated with surface cyclogenesis

-  Forecast premise for mesoscale banding:
-  Requires a _strengthening baroclinic zone_ in the presence of sufficient moisture for precipitation (AND – for snow, the proper thermal stratification).
-  Large-scale deformation zones are BY FAR AND AWAY the most common means of manifesting areas of frontogenesis within the 850-500mb layer.
-  Does _**NOT**_ require a strong surface cyclone, only a low-mid tropospheric baroclinic zone

**Notes:**
F DOES NOT require a strong surface cyclone, only a baroclinic zone (this fact can lull the forecaster into neglecting heavy snow potential (see Moore and Blakley, 1988). This is also why F only rarely plays an important role as a forcing mechanism in the warm season.

## I. CYCLOGENETIC PATTERN

- Mature Stage

- Decaying Stage

*NW of surface cyclone --“wrap around precipitation”*

## Northwest of Strong Cyclone 1/6/02

**Northwest of Strong Cyclone 1/6/02**

## Snowfall Accumulations 

**Snowfall Accumulations**** **

## II. Frontal / Weak Cyclogenesis Pattern

-   Confluent flow ~700mb in advance of a positive tilt trough.
-   Weak or non-existent surface wave cyclone along surface front.
-   Seems to be most common in the Central and Northern Plains with     	quasi-stationary arctic boundaries.

## Within Strong E-W Frontal Zone3/13/02

## Example Case of Frontogenesis and Banded Precipitation

**Date: 15 October 2001 (Case #1)**
- Narrow band (1-2 counties wide) of moderate to heavy rainfall from eastern KS to central IL.
- Associated with weak surface features but a moderately strong baroclinic zone and frontogenesis forcing.

## 700mb 00z 15 OCT 01

**700mb 00z 15 OCT 01**

## Surface 15 OCT 2001

**12z**

**00z**

## 925mb 12z 15 OCT 01

- Large-scale deformation field - eastern KS and western MO

## 18z 15 OCT 01

- 18z 600mb Frontogenesis

- 18z mosaic base reflectivity and surface observations

##  Rainfall rates between 0.10” and 0.25” occurred for a 6 hour period from 15-20z. 

-  Rainfall rates between 0.10” and 0.25” occurred for a 6 hour period from 15-20z.
-  Moderate to heavy precipitation can persist longer (12+ hours) with slower moving systems or mature extratropical cyclones.

## Topeka, KS 12z 15 OCT 01

## 700mb Frontogenesis / Base Reflectivity

- 0 hr ETA 12z

- 6 hr ETA 18z

- 1150z

- 1805z

-  Organization of precipitation increases as F orientation becomes aligned with isotherm orientation at lower levels.

## Sloped Continuity of F

- 6hr ETA forecast valid
- 18z 15 OCT 01

-  Presence of parallel axes of positive frontogenesis sloping upward toward colder air is a common aspect of heavy banded precipitation areas.

- 600 mb

- 700 mb

- 850 mb

## Sloped Continuity of F

- The plane of the cross-section should be taken perpendicular to the mid-level (850-500mb) thermal wind vector or thickness lines.

## Sloped Continuity of Frontogenesis Forcing (cont.)

- The previous two slides have several important implications:
- Several levels (or a x-section) should be assessed for spatial continuity and orientation of *F*, to see if banding is likely to occur at a given time.
- Vertical averaging should probably be avoided.
- The sloped continuity tells us something about the structure of the wind field we can use to infer frontogenesis from single sounding (observed or model derived), VAD, or wind profiler data, and large-scale flow fields.

## Role of Deep-Layer Shear Profile

- Nature of environmental wind profile may be conducive to “seeder-feeder” mechanism and rapid precipitation generation / elongation of bands during initial development phase.

## Role of Deep-Layer Shear (cont.)

- Martin (1998)

-  Note banding orientation (parallel to isentropes / isotherms).

## Vertical Wind Profile and banding

*Idealized Hodographs:*

********* ******Col point aloft***

## Mesoscale Band Variations 

* **Band movement (short and long-axis translation)*
* **Warm season vs. cool season bands*
* **Multiple parallel bands (stability driven)*
*- Non-banded (the “null wind structure”)*

## Banded – Cold Season 3-10Z  12/29/02

## Mosaic Radar 8z  12/29/02

* **RUC 2h frontogenesis forecast 850mb*

## 1.5o Base Velocity / VAD – Spokane, WA0854z 12/29/02

*Frontogenesis** coincident with col point / straight shear *

## Banded – Warm Season 12Z  6/27/01

*Training thunderstorms, in gravitationally unstable environment*

- TLX 1459Z

- VIS 1500Z

## Banded – Translation along short axis North Dakota 0256z  1/26/03

*Two problems for heavy precip:*
*Moisture starved, and moving fast*

## Non-Banded 0256z  12/25/02

## Non-Banded 0256z  12/25/02

*Note strong curvature to the shear vector with height. This tends to preclude coherent banding, even in the presence of frontogenesis. *

## Banded- Multiple 11/09/00

- INX 0903Z

- Montgomery Co.                         

- Unlike Case #1, this case shows narrow multiple banded precipitation. Lower stability likely played a role.

## 700-500mb Lapse Rate Comparison

- Near neutral or unstable lapse rates (with respect to a moist adiabat) implies **multiple** narrow and intense (maybe 5-10 km or so in width), bands. Resulted in 2-3”/hr snowfall rates on Nov 9, 2000.

- 7.8 C/km

- 4.5 C/km

- SGF 12z
- 11/09/00

- TOP 12z
- 10/15/01

## Modulation of Band Intensity by Instability for a constant value of F

- As gravitational or symmetric stability decreases, the horizontal scale of the band decreases while the intensity of the band increases. Multiple bands become established in an unstable regime.

## Using EPV to Measure Stability

-  *EPV = Equivalent Potential Vorticity*
-  A relatively simple, quick, and effective way to evaluate CSI/MSI. Gravitational instability may also be present.
- Defined by Moore and Lambert (1993) as follows:

- (TERM 1)

- (TERM 2)

-  The closer EPV is to zero, the more responsive the atmosphere will be to a given amount of forcing.
-  IF EPV<0 , then CSI/MSI is present. Overlaying EPV with theta-e is an effective way to determine if convective (gravitational) instability also exists.

## Using EPV to Measure Stability

- An example from Moore and Lambert (1993)

## Frontogenesis and Symmetric Instability

**Notes:**
Assent in a saturated environment trends the theta-e lines so that they are oriented more vertically. The condition for Conditional Symmetric Instability (CSI) is that the theta-e lines be more steeply sloped than the geostrophic momentum surfaces locally. Therefore, frontogenesis is generally favorable to bring this situation about. However, is is unlikely that the instability can persist for very long in the presence of lift. The instability is likely used as quickly as it is created, and therefore, the Mg/theta-e lines are more likely to be parallel (neutral with respect to symmetric stability/instability). It is important to keep in mind that the frontogenesis process represents the forcing mechanism.
Instability can only act to modulate the intensity or character of the precipitation area resulting from the forcing. 

## Cloud-Layer Stratificaiton Comparison

- MT

- ND

- 0018Z 22 Oct 02

- 21z RUC Forecast valid at 00z

- 2-D 750mb frontogenesis

*Bismarck VAD *

## ETA 0h EPV 00z 10/22/02

- 0018Z 22 Oct 02

- 700mb (thick dashed line)
- 600mb (thin dashed line)

*Multiple bands exist here in negative EPV regime over Montana.*

## 00z Soundings 10/22/02

- 850-500mb lapse rate: 3.5 C/km

- 700-500mb lapse rate: 6.7 C/km

- 700-500mb lapse rate: 5.1 C/km

*Great Falls, MT*

*Bismarck, ND*

## Numerical Model Considerations

**Date: 7 February 2003 (Case #2)**
- Heavy snow band across southern New England
- QPF/ 700mb UVV field: may not tell you what you need to know, even for a “well-handled” system:
- “What you see isn’t always what you get”

## 2/7/03 09Z RUC Forecast QPF/UVV

## 2/7/03 09Z RUC Forecast 700mb Warm Advection

## 2/7/03 Mosaic Radar 1215z-0022z

## 2/7/03 Mosaic Radar / RUC 700mb F

## Profiler – Plymouth, MA

## Boston, MA Surface Observations

***BOS 13 UTC  1 1/2SM –SN***
***BOS 14 UTC  1/2  SM  SN***
***BOS 15 UTC  1/2  SM  SN  SNINCR 1/ 2***
***BOS 16 UTC  1/2  SM  SN  SNINCR 1/ 3***
***BOS 17 UTC  1/2  SM  SN  SNINCR 2/ 4***
***BOS 18 UTC  1/4  SM +SN  SNINCR 2/ 6***
***BOS 19 UTC  1/4  SM +SN  SNINCR 2/ 8***
***BOS 20 UTC  1/4  SM +SN  SNINCR 2/10***
***BOS 21 UTC  1/4  SM  SN  SNINCR 1/10***
***BOS 22 UTC  1/4  SM -SN ***
***BOS 23 UTC  2    SM –SN***
***BOS 00 UTC  10   SM***

*700 mb*
*F, 18Z*

## Snowfall Accumulations 2/7/03

* **Inadequate resolution likely precluded evidence of band in UVV / QPF fields. *

## Suggested Snow Band Checklist

*Presence of (1”/hr):*
*	**limited dry air advection in near surface.*
* **	**near saturated / high low-mid level RH present (east **	**CONUS, 1000-500mb >85%)*
* **	**Favorable thermodynamic profile for snow (i.e. cloud **	**top temp <-9C, no melting layers)*
*   **	**Sloped region of mid-level 2-D frontogenesis / **	**Deformation axis in 850-500mb range*
*      **	**Relative minimum in wind speed (<20kt) within 850-**	**700mb region (col point aloft) and/or uniform deep-**	**layer shear profile absence of substantial hodograph **	**curvature*

## Suggested Snow Band Checklist (cont.)

*Enhancement of (1-3”/hr, 5”/hr in extreme cases):*
*	**Saturation through dendrite growth layer (-12 to –**	**16C) coincident with strong UVV**	**(high precipitation **	**efficiency) *
* **	**Presence of negative EPV, elevated potential  or **	**slantwise instability (convective snow potential, band **	**multiplicity) *

## SUMMARY

**SUMMARY**

- When applied within the context of ingredients based forecasting, frontogenesis is useful for assessing potential for mesoscale banded precipitation areas.
- Doesn’t require a strong cyclone, only a strong baroclinic zone, often developed through horizontal deformation and associated w/ a col point aloft
- Col point aloft = YOUR cue to investigate F and banding potential
- Location of col point aloft = approximate band location
- Banding is modulated by wind structure and stability
- Banding is not always represented by the models