# Presentation: 023035

## The Anatomy of CSI

- A Cold Case

## Ingredients and Mechanisms for Heavy Snow

** ****Deep layer moisture**: from the surface – 500 mb
-  **A** **vertical temperature profile** conducive to the efficient production of dendritic crystals, high snow:liquid equivalent ratios, and little/no melting of crystals
-  **A slow-moving system** with upstream propagation (i.e., new cloud/precipitation development upwind)
** ****Instability**: not required for light snow (2-4 inches) but definitely needed for heavy banded snowfall

**Ingredients and Mechanisms for Heavy Snow**

-  Convective Instability
-  Inertial Instability
-  Potential Symmetric Instability
-  Conditional Symmetric Instability
-  Weak Symmetric Stability

## Spectrum of Mesoscale Instabilities

**Many heavy precipitation events display different types of mesoscale instabilities including: **

**Convective Instability** (CI; e decreasing with height)

**Conditional Symmetric Instability** (CSI; lines of e  are more vertical than lines of constant absolute geostrophic momentum or Mg)

**Weak Symmetric Stability** (WSS; lines of e are nearly parallel to lines of constant
- absolute geostrophic momentum or Mg) (but still can result in banded precipitation in
- the presence of frontogenetical forcing)

**Notes:**
Many heavy precipitation events display different types of mesoscale instabilities including: 

Convective Instability (CI; e decreasing with height) 

Conditional Symmetric Instability (CSI; lines of e  are more vertical than lines of constant absolute geostrophic momentum or Mg) 

Weak Symmetric Stability (WSS; lines of e are nearly parallel to lines of constant absolute geostrophic momentum or Mg) (but still can result in banded precipitation in the presence of frontogenetical forcing) 
For PSI, we use e and Mg surfaces 

For CSI, we use es and Mg surfaces (saturated e) 

You should display relative humidity on the cross section since CSI requires near- saturated conditions (i.e., RH > 80%) 

There should also be large scale vertical motion in order to “realize” (release) the CSI 

Note: when the e surfaces “fold” underneath themselves, i.e., e decreases with height, there is convective instability, which could result in upright convection and subsequent vertical motions that would overwhelm motions from slantwise convection resulting from the release of CSI

## What is CSI?

- Conditional Symmetric Instability is just that...an instability. It is not a forcing mechanism, or a type of convection (although the term is often misused in that sense)
- CSI is characterized by weak **inertial stability** and **convective stability** but, when realized by a forcing mechanism, results in **slanted or tilted mesoscale circulations** which convert inertial energy into buoyant energy

## Diagnosing Inertial and Convective Stability

**Convective Stability **typically diagnosed
- where:
- 		dθ/dp < 0
**Inertially unstable**** **regions are typically diagnosed where:
- 	     absolute geostrophic vorticity < 0
**Under certain conditions, we can use the absolute geostrophic momentum (Mg) to analyze inertial instability. This is typical in environments with strong speed shear and weak directional shear, where the contours of ****Mg are horizontal on a cross section. **

**Notes:**
The atmosphere likes to remain in geostrophic balance, and when altered, attempts to return to a balanced state. 

## Typical CSI Sounding

**Notes:**
Rawinsonde oservations for IAD for 1200 UTC 26 February 1993:
Region of CSI is above 600 mb in this case

## Conditional Symmetric Instability: Synoptic Characteristics

- Typically a cool season phenomena
**Wind profile:** speed increasing with height and weak directional veering with height; indicative of strong baroclinicity
**Thermodynamic profile:** nearly saturated and close to the moist-adiabatic lapse rate.  Parcel motion will be neutral to moist ascent. Lapse rate is NOT conditionally unstable
- Often found in the vicinity of a extratropical cyclone warm front, ahead of long-wave troughs in regions of strong, moist, mid-tropospheric southwesterly flow
- Large scale forcing for upward vertical motion is usually present

## Slide 8

## Diagnosing Potential Symmetric Instability (PSI) and Conditional Symmetric Instability (CSI)

**Construct a cross section taken normal to the 850-300 mb thickness isopleths with the x axis directed towards the warm air. **
**In the cross-sectional plane display isentropes of ****θ****e/ ****θ****es and isopleths of absolute angular momentum (Mg), defined as: **
- Mg = vg + fx , where vg is the geostrophic wind component normal to the cross section, f is the Coriolis parameter, and x is the distance along the x axis.
**Note that ****θ****e/****θ****es tends to increase both upward (in convectively/conditionally stable air) and along the x axis (towards the warmer air); Mg tends to increases both upward (as the normal wind component increases with height) and along the x axis (as x increases) **

## Diagnosing PSI/CSI (cont.)

**For PSI we use ****θ****e and Mg surfaces. **
**For CSI we use ****θ****es and Mg surfaces. **
**You should display relative humidity on the cross section since CSI requires near- saturated conditions (i.e., RH > 80%) **
**There should also be large scale vertical motion in order to “realize” the CSI. **
**Note: when the ****θ** **e  surfaces “fold” underneath themselves there is convective instability.**

## e 

- e

- Mg +1

- e+ 1

- e-1

- Mg

- Mg -1

- In this diagram, isentropes of e are sloped more vertical than lines of absolute geostropic momentum, Mg.  This implies weak stability (**vertical ********e**** lines mean neutral stability while more horizontal lines mean increased stability**) and decent vertical speed shear (Mg lines that are nearly vertical implies near constant wind speeds with height; **the more horizontal the M surfaces, the greater the vertical wind shear and better chance for CSI**).** **

_**Parcel A (as it’s displaced horizontally to the NW) **_
******e (parcel)  > ********e (environ);  ******** dw/dt  >  0  (accel. up) **
**M g (parcel) > M g (environ); ********  du/dt >  0   (accel. to southeast) **

**Understanding Conditional Symmetric Instability**

_**Parcel B (as it’s displaced vertically upward) **_
******e (parcel)  < ********e (environ);  ******** dw/dt  <  0  (accel. down) **
**M g (parcel) < M g (environ); ********  du/dt <  0   (accel. to northwest) **

_**Parcel C (as it’s displaced slantwise up and from SE to NW) **_
******e (parcel)  > ********e (environ);  ******** dw/dt  >  0  (accel. up) **
**M g (parcel) < M g (environ); ********  du/dt  <  0   (accel. to northwest) **

**Thus, ****Parcel C will accelerate along a slantwise path away from its initial position****....it is unstable to ****slantwise motions ****even though it is somewhat stable to both horizontal and vertical displacements!**

**Notes:**
In this diagram, isentropes of e are sloped more vertical than lines of absolute geostrophic momentum, Mg.  This implies weak stability (vertical e lines mean neutral stability while more horizontal lines mean increased stability) and decent vertical speed shear (Mg lines that are nearly vertical implies near constant wind speeds with height; the more horizontal the M surfaces, the greater the vertical wind shear and better chance for CSI). 

Parcel θe and Mg properties are those of parcel at its original location before displacement; after displacement, parcel travels through environment with certain environmental θe and Mg properties 
Parcel A (as it’s displaced horizontally to the NW) 
e (parcel)  > e (environ);   dw/dt  >  0  (accel. up) 
M g (parcel) > M g (environ);   du/dt >  0   (accel. to southeast...but eventually returns to near original location) 
Parcel B (as it’s displaced vertically upward) 
e (parcel)  < e (environ);   dw/dt  <  0  (accel. down) 
M g (parcel) < M g (environ);   du/dt <  0   (accel. to northwest) 
Parcel C (as it’s displaced slantwise up and from SE to NW) 
e (parcel)  > e (environ);   dw/dt  >  0  (accel. up) 
M g (parcel) < M g (environ);   du/dt  <  0   (accel. to northwest) 
Thus, Parcel C will accelerate along a slantwise path away from its initial position....it is unstable to slantwise motions even though it is somewhat stable to both horizontal and vertical displacements!

## Conditional Symmetric Instability: Physical Characteristics

- Width of the bands is approximately 50-100 km; length of the bands is approximately 100-400 km; time scale of the bands is approximately 3-4 h
- Typical CSI vertical motions are on the order of  tens of cm s-1 to a few m s-1 and thus, usually DO NOT produce lightning/thunder (need > 5 m s-1 to produce lightning)
- However, these mesoscale bands of precipitation can be intense and result in significantly higher rain/snow fall totals than the surrounding area
- CSI can be assessed using a parameter called the **Equivalent Potential Vorticity (EPV)** – values less than 0.25 PVU indicate regions susceptible to CSI

## Conditional Symmetric Instability: Observational Characteristics

- On satellite or radar imagery CSI is exhibited by multiple bands of clouds/precipitation oriented parallel to the mid-tropospheric thermal wind (or thickness lines); sometimes the bands have a component of motion toward the warm air
- These heavier precipitation bands may be embedded (obscured) by other lighter precipitation
- Warm frontal rain/snow bands are often good candidates for being associated with CSI

## Conditional Symmetric Instability: A Summary

- The atmosphere can contain regions of CSI and convective instability (CI), but since CI has a faster growth rate (tens of minutes) relative to CSI (a few hours), it will dominate.
- CSI is favored to occur in regions of:
- High vertical wind shear
- Weak absolute vorticity  (values near zero)
- Weak convective stability
- High mean relative humidity
- Large scale ascent
- These conditions are often found in the entrance region of an upper-level jet streak during the cold season

## Equivalent Potential Vorticity (EPV)

-  Equivalent Potential Vorticity (EPV) is a parameter that can be used to diagnose areas of CSI.
-  You want to find areas of negative or small positive EPV.
-  The stronger the e gradient from south to north and greater the vertical wind speed shear, the smaller (less positive or more negative) EPV will be.
-  EPV is small within ridge axes, south of jet streaks, and often in dry slots.
-  When EPV < 0, potential symmetric instability (PSI) is present. Schultz and Schumacher (1999 MWR) suggest using es (saturated e instead of regular e) to assess CSI.  However, it is perfectly acceptable to use e and check to be sure that the relative humidity is greater than 80 percent.
-  However, EPV also is < 0 when there is convective instability (CI), i.e., when e decreases with height (e lines are bent back or “folded” on a cross-section). If so, CI will dominate which could lead to upright convection given adequate forcing. CI typically is located south of an area of CSI/PSI.

## Differential moisture advection northeast of the surface low (in the previous diag.) leads to a steepening of the θe/θes surfaces. 

**Mid-level frontogenesis increases the north-south thermal gradient, thereby increasing the vertical wind shear. In this case the easterlies increase below while the westerlies increase above – which increases the differential moisture advection, increasing the ?e/ ?es surfaces’ slope. **

**Nicosia and Grumm (1999, WAF) Conceptual Model for CSI**

## Also....since the vertical wind shear is increasing with time the Mg surfaces become more horizontal (become flatter). Thus, a region of PSI/CSI develops where the θe/θes surfaces are more vertical than the Mg surfaces. 

**In this way frontogenesis and the develop- ment of PSICSI are linked. **

**Nicosia and Grumm (1999, WAF) Conceptual Model for CSI**

## Nicosia and Grumm Model for EPV Reduction Near Extratropical Cyclones

**Nicosia and Grumm Model for EPV Reduction Near Extratropical Cyclones**

**Nicosia and Grumm (1999, WAF) proposed a conceptual model in which a zone of EPV reduction in **
**concert with an area of mid-level frontogenesis will aid in the prediction of mesoscale bands of snow.**

## Problems in Diagnosing CSI Operationally

**Temporal Resolution:**** CSI occurs over time scales of about 3-6 hours while current upper air data collection is every 12 hours **
** **
**Spatial Resolution:**** Precipitation bands are meso-******** scale with lengths of 100-200 km and widths of 50-100 km **
**Geostrophic assumption**** is not always valid (e.g., in regions of cyclonic curvature or within ULJ exit/entrance regions). **
**When the shear vector turns with height, the inertial stability criteria is no longer valid for some portions of the cross section; M****g**** is not strictly conserved **

**Nevertheless, a forecaster can ****anticipate**** when/where CSI might occur from**
**looking at model and observed data (situational awareness). Then in the short term, when banded precipitation is noted, physical processes responsible can be understood, and the forecast adjusted as needed to refine precipitation amounts **

## As gravitational or symmetric stability decreases, the horizontal scale (width) of a precipitation band decreases while the intensity (reflectivity) of the band increases. Multiple bands become established in an unstable regime.  Thus, it is very important to look for CSI and convectively unstable areas aloft besides just frontogenesis. 

**Notes:**
Precipitation within areas of frontogenetical forcing can organize into bands
These bands become more numerous and intense when instability is present (either convective instability or CSI)
Numerical experiments suggest that weak positive symmetric stability (WSS) in the warm air in the presence of frontogenesis leads to a single band of ascent that narrows as the symmetric stability approaches neutrality 

Also, if the forcing becomes horizontally widespread and EPV < 0, multiple bands become embedded within the large scale circulation; as the EPV decreases, the multiple bands become more intense and more widely spaced 

## NW

**NW**

**SE**

- NW-SE cross-section shown on next slide.

**A Conceptual Model: Plan View of Key Processes**

- CI tends to be in the warmer air to the south of the cyclone while CSI and
- WSS tend to develop further north in the presence of a cold, stable boundary layer

- Often found in the vicinity of an extratropical cyclone warm front, ahead of a long-wave trough in a region of strong, moist, mid-tropospheric southwesterly flow** **

## Dry Air

**Dry Air**

******es**** **

**Convectively Unstable **

**Shaded area = CSI**

**CSI**

**Arrows = Ascent zone **
**F = Frontogenesis zone**

**Heavy snow area**

**A Conceptual Model: Cross-Sectional View of Key Processes**

- CSI may be a precursor to elevated CI, as the vertical circulation associated with CSI may overturn e surfaces with time creating convectively unstable zones aloft

- It is not unusual to see CI move north and become elevated, producing thundersnow

- Most thundersnow events are associated with elevated convective instability (as opposed to CSI)

**Notes:**
These mesoscale instabilities tend to develop from north to south in the presence of strong uni-directional wind shear (typically from the SW) 

CI tends to be in the warmer air to the south of the cyclone while CSI and WSS tend to develop further north in the presence of a cold, stable boundary layer 

It is not unusual to see CI move north and become elevated, producing thundersnow 

CSI may be a precursor to elevated CI, as the vertical circulation associated with CSI may overturn e surfaces with time creating convectively unstable zones aloft 

These mesoscale instabilities tend to develop from north to south in the presence of strong uni-directional wind shear (typically from the SW) 

CI tends to be in the warmer air to the south of the cyclone while CSI and WSS tend to develop further north in the presence of a cold, stable boundary layer 

It is not unusual to see CI move north and become elevated, producing thundersnow 

CSI may be a precursor to elevated CI, as the vertical circulation associated with CSI may overturn e surfaces with time creating convectively unstable zones aloft 

We believe that most thundersnow events are associated with elevated convective instability (as opposed to CSI) 

CSI can generate vertical motions on the order of 1-3 m s-1 while elevated CI can generate vertical motions on the order of 10 m s-1 which are more likely to create charge separation and lightning 

NOTE:  Given model resolution, it may be difficult at times to fully and accurately resolve small-scale zones of elevated CI, CSI, or WSS in vertical cross-sections; keep this in mind when assessing instability  
There should also be large scale vertical motion in order to “realize” (release) the CSI 

Note: when the e surfaces “fold” underneath themselves, i.e., e decreases with height, there is convective instability, which could result in upright convection and subsequent vertical motions that would overwhelm motions from slantwise convection resulting from the release of CSI