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Synoptic Meteorology-II > chapter 2: Analysis of Mid-latitude Synoptic Scale Systems using QG Height Tendency Equation > Flashcards

chapter 2: Analysis of Mid-latitude Synoptic Scale Systems using QG Height Tendency Equation Flashcards

1
Q

The QG Height Tendency Eq. can be expressed as:

A
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2
Q

the equation is a

A

partial differential equation describing the local change of the geopotential height (Φ) on an isobaric surface with respect to time

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3
Q

There are three forcing terms on the right-hand side of The QG Height Tendency Eq. From left to right, these forcing terms represent:

A
  1. Geostrophic vorticity advection
  2. Differential thermal advection and
  3. Differential diabatic heating.
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4
Q

The QG Height Tendency Eq. is applied to

A

the study of troughs and ridges in the middle troposphere – often at 500 hPa – and not at the surface

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5
Q

The contribution to the local geopotential height tendency exclusively due to geostrophic vorticity advection can be expressed by:

A
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6
Q

The contribution to the local geopotential height tendency exclusively due to geostrophic vorticity advection can be expressed by:

It depicts the

A

advection by the geostrophic wind of the geostrophic relative (عg) and planetary vorticity (f)

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7
Q

Cyclonic geostrophic vorticity advection will result in

A

local decrease in geopotential height with time

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8
Q

Cyclonic geostrophic vorticity advection will result in local decrease in geopotential height with time, because:

A
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9
Q

Cyclonic geostrophic vorticity advection will result in local decrease in geopotential height with time, because:

A
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10
Q

Cyclonic geostrophic vorticity advection will result in local decrease in geopotential height with time, because:

A
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11
Q

Anticyclonic geostrophic vorticity advection will result in

A

local increase in geopotential height with time

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12
Q

Anticyclonic geostrophic vorticity advection will result in local increase in geopotential height with time, because:

A
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13
Q

Anticyclonic geostrophic vorticity advection will result in local increase in geopotential height with time, because:

A
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14
Q

Anticyclonic geostrophic vorticity advection will result in local increase in geopotential height with time, because:

A
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15
Q

In an idealized trough/ridge scenario where the geostrophic wind is

A

uniform everywhere

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16
Q

In an idealized trough/ridge scenario where the geostrophic wind is uniform everywhere and thus geostrophic relative vorticity is ………………………. in the base ……………………………

A

maximized

of each trough

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17
Q

In an idealized trough/ridge scenario where the geostrophic wind is uniform everywhere and thus geostrophic relative vorticity is ………………………….. in the apex …………………………..

A

minimized

of each ridge

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18
Q

In an idealized trough/ridge scenario where the geostrophic wind is uniform everywhere and thus geostrophic relative vorticity is maximized in the base of each trough

Thus, there is an …………………………… geostrophic vorticity advection to the ……………………………… axis

A

anticyclonic

west of the trough

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19
Q

In an idealized trough/ridge scenario where the geostrophic wind is uniform everywhere and thus geostrophic relative vorticity is (minimized) in the (apex) of each (ridge).

Thus, there is an ……………………. geostrophic vorticity advection to the…………………………….

A

(cyclonic)

west of the trough axis

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20
Q

n an idealized trough/ridge scenario where the geostrophic wind is uniform everywhere and thus geostrophic relative vorticity is maximized in the base of each trough

Thus, there is an anticyclonic geostrophic vorticity advection to the west of the trough axis, which is associated with a tendency for height …………

A

rises

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21
Q

In an idealized trough/ridge scenario (Fig.1), where the geostrophic wind is uniform everywhere and thus geostrophic relative vorticity is (minimized) in the (apex) of each (ridge).

Thus, there is an (cyclonic) geostrophic vorticity advection to the west of the trough axis, which is associated with a tendency for height ………..

A

falls

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22
Q

A

A
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23
Q

B

A
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24
Q

C

A
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25
Q

D

A
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26
Q

E

A
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27
Q

F

A
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28
Q

G

A
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29
Q

H

A
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30
Q

A

A
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31
Q

B

A
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32
Q

C

A
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33
Q

D

A
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34
Q

E

A
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35
Q

F

A
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36
Q

At the center of a cyclonic vorticity maximum, the height tendency is

A

zero.

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37
Q

Since the geostrophic wind blows

A

parallel to contours of constant geopotential height

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38
Q

Since the geostrophic wind blows parallel to contours of constant geopotential height, geostrophic absolute vorticity advection does

A

not result in the amplification (or intensification) of troughs and ridges.

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39
Q

geostrophic absolute vorticity advection does not result in the amplification (or intensification) of troughs and ridges.

 Rather, it results in

A

their movement from one location to another.

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40
Q

geostrophic absolute vorticity advection does not result in the amplification (or intensification) of troughs and ridges.

 Rather, it results in their movement from one location to another. This is identical to the interpretation offered with

A

the quasi-geostrophic vorticity equation

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41
Q

When a wind speed asymmetry exists in the vicinity of an upper trough, as shown in the import or export of ……………………………………. can lead to

A

cyclonic shear vorticity can lead to a net height tendency in the base of the trough

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42
Q

A

A
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43
Q

B

A
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44
Q

C

A
45
Q

D

A
46
Q

E

A
47
Q

F

A
48
Q

G

A
49
Q

The following represents a

A

digging trough

50
Q

A

A
51
Q

B

A
52
Q

C

A
53
Q

D

A
54
Q

E

A
55
Q

F

A
56
Q

The following represents a

A

lifting trough

57
Q

Digging Trough

In the case where a jet streak is located to the

A

west of the trough axis

58
Q

Digging Trough

 In the case where a jet streak is located to the west of the trough axis, as in Fig.3a, there is a

A

net import of cyclonic vorticity into the base of the trough

59
Q

Digging Trough

 In the case where a jet streak is located to the west of the trough axis, as in Fig.3a, there is a net import of cyclonic vorticity into the base of the trough, and we expect

A

the trough to amplify and dig equatorward toward lower latitudes

60
Q

In the case where a jet streak is located to the west of the trough axis, as in Fig.3a, there is a net import of cyclonic vorticity into the base of the trough, and we expect the trough to amplify and dig equatorward toward lower latitudes.

 Such a trough configuration is commonly referred to as a

A

“digging” trough

61
Q

wind speed maximum on the downstream side of the trough leads to

A

a net export of vorticity

62
Q

In contrast, a wind speed maximum on the downstream side of the trough leads to a net export of vorticity, leading to a

A

a weakening and poleward movement of the trough

63
Q

In contrast, a wind speed maximum on the downstream side of the trough leads to a net export of vorticity, leading to a weakening and poleward movement of the trough; this is known as a

A

“lifting” trough

64
Q

A process that is often strongly linked to the amplification or decay of upper- level troughs and ridges is represented by the

A

differential thermal advection term

65
Q

A process that is often strongly linked to the amplification or decay of upper- level troughs and ridges is represented by the differential thermal advection term in The QG Height Tendency Eq.

A
66
Q

the term involves the

A

vertical derivative of thickness advection

67
Q

This term involves the vertical derivative of thickness advection and represents

A

thickness tendency that would accompany a given sign of temperature advection within an atmospheric layer.

68
Q

A

A
69
Q

B

A
70
Q

C

A
71
Q

D

A
72
Q

E

A
73
Q

F

A
74
Q

A

A
75
Q

B

A
76
Q

C

A
77
Q

D

A
78
Q

E

A
79
Q

The images explain

A

Geopotential height changes associated with the differential thermal advection

80
Q

Warm advection

Suppose a …………………….. of warm advection is located…………………………..

A

maximum

near the 700-mb level

81
Q

If the column experiences net warming due to this process, the

A

thickness of the layer must increase.

82
Q

The sign of the height tendency depends on

A

whether the pressure surface in question lies above or below the level of maximum thermal advection

83
Q

The sign of the height tendency depends on whether the pressure surface in question lies above or below the level of maximum thermal advection:

A
  • Height raises above the level of maximum warming.
  • Height falls below the level of maximum warming.
  • For a pressure surface located exactly at the level of maximum thermal advection, the height tendency would be zero.
84
Q

A similar interpretation applies to ………………….. of cold advection in the …………….

A

a local maximum

lower troposphere

85
Q

A similar interpretation applies to a local maximum of cold advection in the lower troposphere (Fig. 4b); only the signs of the height tendency are

A

reversed relative to those in the warm-advection case

86
Q

Differential thermal advection of either sign is frequently observed in

A

the vicinity of midlatitude cyclones

87
Q

Warm advection to the ………………………………………….. is often associated with

A

east of such systems (ahead of a warm front)

pressure falls in the lower troposphere and a building of an upper ridge downstream of the system.

88
Q

Behind the surface cold front to the

A

west of a cyclone, lower-tropospheric cold advection

89
Q

Behind the surface cold front to the west of a cyclone, lower-tropospheric cold advection is consistent with

A

rising surface pressure and falling upper-level geopotential height surfaces.

90
Q

The role of the diabatic term in Eq.(1) is similar to that of

A

the thermal advection

91
Q

Diabatic warming…………………………. increases with ………………

A

J =dQ/dt

hight

92
Q

Diabatic warming increasing with height leads to ……………. , implying a ………………………………

A

x < 0

local decrease in geopotential height with time

93
Q

Conversely, diabatic warming decreasing with

A

height (or diabatic cooling increases with height)

94
Q

Conversely, diabatic warming decreasing with height (or diabatic cooling increases with height), leads to ……… implying a ………………..

A

x > 0

local increase in geopotential height wind time

95
Q

the following is the equation of

A

the QG Height Tendency Eq.

96
Q

the terms are

  1. Geostrophic vorticity advection
  2. Differential thermal advection and
  3. Differential diabatic heating.
A

three forcing terms of the GQ height tendency equation

97
Q

the following equation represents

A

The contribution to the local geopotential height tendency exclusively due to geostrophic vorticity advection

98
Q

………………………………………… will result in local decrease in geopotential height with time

A

Cyclonic geostrophic vorticity advection

99
Q

……………………………………………………………….. will result in local increase in geopotential height with time

A

Anticyclonic geostrophic vorticity advection

100
Q

In an idealized trough/ridge scenario (Fig.1), where the geostrophic wind is uniform everywhere and thus geostrophic relative vorticity is maximized

A

in the base of each trough

thus there is an anticyclonic geostrophic vorticity advection to the west of the trough axis, which is associated with a tendency for hight rises

101
Q

In an idealized trough/ridge scenario (Fig.1), where the geostrophic wind is uniform everywhere and thus geostrophic relative vorticity is minimized

A

in the apex of each ridge

this, there is a cyclonic geostrophic vorticity advection to the west of the trough axis, which is associated with a tendency for hight falls

102
Q

………………………………………………. blows parallel to contours of constant geopotential height

A

the geostrophic wind

103
Q

……………………………………………………. does not result in the amplification (or intensification) of troughs and ridges

A

geostrophic absolute vorticity advection

104
Q

……………………………………………. results in their movement from one location to another

A

geostrophic absolute vorticity advection

105
Q

………………………………………………. is identical to the interpretation offered with …………………………………….

A

geostrophic absolute vorticity advection

the quasi-geostrophic vorticity equation

106
Q

………………………………………………… can lead to a net height tendency in the base of the trough.

A

wind speed asymmetry exists in the vicinity of an upper trough

the import or export of cyclonic shear vorticity

107
Q

…………………………………………………………… is represented by the differential thermal advection term

A

A process that is often strongly linked to the amplification or decay of upper- level troughs and ridges

108
Q

the following is

A

Differential Thermal Advection

Synoptic Meteorology-II (7 decks)

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