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training forecasting (rao) > Chapter 2- Application of Theories > Flashcards

Chapter 2- Application of Theories Flashcards

1
Q

Horizontal divergence can be expressed as:

A
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2
Q

to compute horizontal divergence at (x0, y0) evaluate the derivative using the

A

central finite differences:

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3
Q

Example-1: Calculate the horizontal divergence for the data given in Figure. Given:
∆x=∆y=50km

A
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4
Q

Example-1: Calculate the horizontal divergence for the data given in Figure. Given:
∆x=∆y=50km

Example-2: Repeat the above calculations with small changes (errors) in winds.

A
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5
Q

Divergence estimates using kinematic method areDivergence estimates using kinematic method are

A

very sensitive to small errors

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6
Q

Vorticity is a

A

microscopic measure of rotation at any point in a fluid

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7
Q

Vorticity is a microscopic measure of rotation at any point in a fluid. It may be considered to be

A

the local rotation of a fluid

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8
Q

Vorticity is a microscopic measure of rotation at any point in a fluid. It may be considered to be the local rotation of a fluid. Vorticity is a

A

vector field, which is defined as the curl of velocity

w=-/x V

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9
Q

where v =

A

(iu+ jv+ kw) is a 3d velocity field

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10
Q

-/x V =

A
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11
Q

w=

A
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12
Q

Because horizontal winds are usually larger than

A
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13
Q

Relative vorticity has units of

A

of s-1 and vorticity is defined as positive in the counterclockwise direction

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14
Q

The Earth is rotating about its axis at rate

A

Ω (s-1).

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15
Q

Since winds are defined

A

relative to the Earth’s surface, we express rotation about the Earth’s axis, in terms of those same coordinates, as:

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16
Q

The vertical component of Earth vorticity is called the

A

coriolis parameter, f

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17
Q

Absolute vorticity is

A

the vector combination of relative vorticity (ζ) and Earth vorticity (f):

ζa = ζ +f

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18
Q

absolute vorticity of a fluid parcel is equal to

A

the sum of the (vertical) rotation of the fluid parcel relative to the earth (relative vorticity) and the vertical component of the rotation of the earth at that position.

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19
Q

The gradient of a variable is

A

just the change in that variable as a function of distance

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20
Q

The gradient of a variable is just the change in that variable as a function of distance. For instance,

A

the temperature gradient is just the temperature change divided by the distance over which it is changing: /_\T//_\ distance

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21
Q

The gradient is a

A

vector and has a direction as well as magnitude.

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22
Q

Mathematically, the gradient vector is defined by

A
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23
Q

for example

A
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24
Q

The gradient of a scalar is

A

a vector whose direction is always normal to the isolines (contours) and pointing in the direction of increase

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25
Q

We can define the normal vector, which is just the

A

unit vector in the direction of the increasing temperature. We will call this normal vector n

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26
Q

The magnitude and direction of a 2D gradient vector for T can be determined by:

A
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27
Q

…………………………………….. then the gradient is zero

A

If the scalar is uniform in space

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28
Q

Advection

A

The transport of an atmospheric property (e.g., temperature, humidity), which is variable in space, by wind is called ‘advection’.

29
Q

The transport of an atmospheric property (e.g., temperature, humidity), which is variable in space, by wind is called ‘advection’.
 This transport process plays a very important part in

A

local changes of temperature and moisture, among other atmospheric properties

30
Q

Mathematically, advection is expressed as:

A
31
Q

Theoretically advection can be viewed as

A

three dimensional

32
Q

Theoretically advection can be viewed as three dimensional. In operational
meteorology the term advection is typically limited to

A

transport by the horizontal flow while vertical transport is called convection

33
Q

In Cartesian coordinates, horizontal advection is given by

A
34
Q

Example: The wind is from 330° at 25 m/s. The isotherms are oriented north-south as shown in the picture below, and are 100 km apart.

A
35
Q

For a thin layer, the geostrophic temperature advection is given by:

A
36
Q

Troughs

A

Troughs which are the regions of low pressure are produced by large volumes of cool or cold air while large volumes of warm or hot air produce ridges, which are the regions of high pressure.

37
Q

The winds on upper level charts blow

A

parallel to the contour lines generally from west to east

38
Q

The winds on upper level charts blow parallel to the contour lines generally from west to east.
 This is a little difference from

A

surface winds which blow across the isobars toward low pressure

39
Q

Temperature drops as you move from

A

west to east and from south to north

40
Q

For example, the highest point on the 850 mb surface (………….. m or so) is found above

A

1800

the hot air near the SW corner

41
Q

For example, the highest point on the 850 mb surface (1800 m or so) is found
above the hot air near the SW corner. The lowest point

A

(a little less than 1000 m) is found in the coldest air near the NE corner of the picture.

42
Q

The above distribution of height contours can be explained by noting that:

A

(1) pressure decreases with increasing altitude, and
(2) pressure decreases more rapidly in cold high-density air than it does in warm low-density air.

43
Q

The counterclockwise winds spinning around the LOW move

A

warm air northward and cold air southward

44
Q

The counterclockwise winds spinning around the LOW move warm air northward and cold air southward.
 Warm air is found

A

west of the HIGH and to the east of the LOW. This is where the two ridges on the upper level chart are also found.

45
Q

Warm air is found west of the HIGH and to the east of the LOW. This is where the two ridges on the upper level chart are also found.
 Similarly, cold air is found

A

below an upper level trough.

46
Q

The yellow Ox marked on the upper level chart directly above the surface L is

A

a good location for a surface LOW to form, develop, and strengthen (strengthening means the pressure in the surface low will get even lower; this is also called “deepening”).

47
Q

The reason for this is that the yellow Ox is a location where there is often

A

upper level divergence

48
Q

Similarly, the pink Ox is where we often find

A

upper level convergence

49
Q

Similarly, the pink Ox is where we often find upper level convergence. this causes

A

the pressure in the center of the surface high to get even higher.

50
Q

The area around a jet streak can be divided into four quadrant relative to the

A
51
Q

it can be shown dynamically that for …………………………………….. are areas of divergence

A

straight flow in the upper troposphere, the left front and right rear quadrants (C and D)

52
Q

are areas of divergence while …………………………….. are areas of convergence

A

right front and left rear quadrants (D and A)

53
Q

Areas of divergence in the upper troposphere are typically associated with

A

upward synoptic scale vertical motion

54
Q

area of upper level convergence are typically associated with

A

downward synoptic scale vertical motion

55
Q

Where upper level convergence occurs air

A

sinks to promote high pressure at the surface.

56
Q

Where upper-level divergence occurs air

A

is pulled up from the surface to help create low pressure near the ground.

57
Q

Wave cyclones dissolve when

A

they no longer have the upper level divergence to maintain them

58
Q

The combination of rising and sinking air creates

A

direct and indirect circulations in the rear (AB) and front (CD) regions across the jet stream, respectively

59
Q

Because cyclones need ………………… to maintain themselves

A

divergence in the upper troposphere

60
Q

Because cyclones need divergence in the upper troposphere to maintain themselves, the divergence/convergence regions around the jet streak have

A

direct affect on the surface lows and highs

61
Q

The vorticity pattern associated with a (straight flowing) jet streak show

A

a strong positive relative vorticity maximum to the left of the jet maximum (plus) and a weaker negative relative vorticity minimum to the right ( minus).

62
Q

The location of the vorticity maximum and minimum indicate that there should be

A

positive vorticity advection (PVA) in the left exit and right entrance regions.

63
Q

Quasi-geostrophic theory indicated the PVA is favorable for

A

cyclone development.

64
Q

Hence, the typical location of a intensifying surface low center is in

A

the left exit region

65
Q

while …………………………. are common in the right entrance region.

A

newly formed frontal waves

66
Q

A jet streak moves

A

within the trough-ridge pattern at the same time it influences the amplification or de-amplification of the trough-ridge pattern.

67
Q

Below is an example of a jet streak de-amplifying (weakening) a trough

A

A strong jet streak on the right side of a trough will cause that trough to de-amplify (lift)

68
Q

amplifying (image)

A

If a strong jet streak is on the left side of a trough, the trough will amplify (dig)

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