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Synoptic Meteorology > part 1 > Flashcards

part 1 Flashcards

1
Q

Synoptic meteorology

A

meteorology traditionally involves the study of weather systems, such as

  • extratropical high and low pressure systems,
  • jet streams
  • associated waves
  • fronts.
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2
Q

mesoscale meteorology

A
  • the study of convective storms,
  • land–sea breezes,
  • gap winds,
  • and mountain waves
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3
Q

The earth system exhibits a continuous……………………….spectrum of motion that defies simple categorization.

A

spatial and temporal

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4
Q

Weather forecasting

A

necessitates understanding a wide range of processes and phenomena acting on a variety of spatial and temporal scales.

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5
Q

forecasting for a coastal location requires information concerning

A
  • the near-shore water temperature,
  • the potential for land–sea breeze circulations,
  • and the strength and orientation of the prevailing synoptic-scale wind flow.
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6
Q

The prediction of precipitation type can benefit from

A

knowledge of atmospheric thermodynamics and cloud physics.

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7
Q

Other types of prediction, including ……………………………………… and ……………………………, also require knowledge that spans a broad spectrum of meteorological processes.

A

air quality forecasting and seasonal climate prediction

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8
Q

quasigeostrophic (QG) equations

A

simplified version of the full primitive equations

igoners small terms

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9
Q

momentum equations are

A

continuous

ideal gas

hydrostatic

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10
Q

geostraphic wind is a balance between

A

corriolis and PGF

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11
Q

scale analysis

A

a systematic strategy to determine which terms in the equations, often associated with specific physical processes, are most important and which are negligible in a given meteorological setting.

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12
Q

scale analysis is a systematic strategy to determine which terms in the equations, often associated with specific physical processes, are most important and which are negligible in a given meteorological setting. By

A

characterizing the temporal and spatial scales associated with specific weather systems, we can systematically neglect “small” terms in the governing equations in the study of those systems.

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13
Q

for synoptic- and planetary-scale weather systems, such as cyclones and anticyclones, we know that in the ……………………………, flow above……………………tends to be fairly close to a state of ……………………………balance

A

midlatitudes, ~1 km altitude, geostrophic

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14
Q

—flow above ~1 km altitude tends to be fairly close to a state of geostrophic balance, whereas for mesoscale weather systems, such as thunderstorms, it …………………………………………………….

A

does not, even in the same geographical location

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15
Q

geostrophic balance ignores

A

friction

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16
Q

whereas for mesoscale weather systems, such as thunderstorms, it does not, even in the same geographical location. Why?

A

cannot ignore friction

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17
Q

This is one example of why students in the atmospheric sciences are required to derive equations, because it is important to know what ……..

A
  • assumptions were made in the development of a given technique
  • this information is needed to deduce which tools are appropriate for which situations.
  • the ability to apply a systematic approach to the governing equations allows atmospheric scientists to develop new equations and techniques to study unique problems.
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18
Q

The length scale can be related to

A

the size of a weather system, or how far an air parcel would travel within the system during a given time interval.

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19
Q

The time scale

A

can be related to how long it would take an air parcel to circulate within the system

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20
Q

Scale: Microscale

length:

A

less than 1 km

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21
Q

Scale: Microscale

time:

A

less than 1 hour

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22
Q

Scale: Microscale

example phenomena:

A

Turbulence, PBL

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23
Q

Scale: Mesoscale

Length:

A

1 - 1000 km

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24
Q

Scale: Mesoscale

time:

A

1 h - 1 day

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25
Q

Scale: Mesoscale

example phenomena:

A

Thunderstorm, land-sea breeze

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26
Q

Scale: synoptic

length:

A

1,000-4,000

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27
Q

Scale: synoptic

time:

A

1 day-1 week

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28
Q

Scale: synoptic

Example phenomena:

A

Upper level trough, ridges, fronts surface lows and highs

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29
Q

Scale: Planetary

Lenght:

A

less than 4000 km

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30
Q

Scale: planetary

time:

A

less than 1 week

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31
Q

Scale: planetary

Example phenomena:

A

polar front jet streams, trade winds

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32
Q

the dependent variables in the system

A
  • the four independent variables are the three spatial directions
  • and time, denoted as x, y, z, and t, respectively
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33
Q

governing equations are applied to a flat “cartesian” earth for

A
  • qualitative work,
  • or if we study weather systems that are sufficiently small in spatial scale, we can neglect the distortion that results.
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34
Q

shows unit vectors in an orthogonal Cartesian coordinate system. For some applications, the i and j unit vectors may be

A

grid relative

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35
Q

the horizontal coordinate directions here will be taken to align with

A

latitude and longitude lines

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36
Q

A and B represent

A

K^ (z, + upward)

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37
Q

C and D represent

A

j^ (y, +northward)

38
Q

E and F represent

A

i^ (x, +eastward)

39
Q

omega = dp/dt is (…..) upward

A

negative

40
Q

w=dz/dt is (…….) upward

A

positive

41
Q

a variety of vertical coordinates measures are used in place of the ……….

A

vertical distance z

42
Q

a variety of vertical coordinate measures are used in place of the vertical distance z to determine …..

A

determine position along the vertical coordinate axis

43
Q

popular choice of vertical coordinates

A

pressure, sigma (a terrain-following ratio of pressure to surface pressure), potential temperature, or a hybrid among these

44
Q

the k unit vector maintains

A

right angles with the horizontal unit vectors.

45
Q

vertical coordinates are known as……

A

isobaric coordinates

46
Q

an important practical advantage is that historically, it was easier to measure ……………………………. than ……………………….for in situ measurements taken aloft.

A

pressure than altitude

47
Q

a rawinsonde can measure

A

pressure with a baroswitch

48
Q

aircraft are designed to measure

A

pressure and fly along surfaces of constant pressure

49
Q

The wind velocity components are based on

A

the time rate of change in the distance along the respective coordinate axes following the airflow

50
Q

Wind velocity components (equations)

A
51
Q

The following are the

A

wind velocity components

52
Q

dx/dt indicates

A

change in zonal (east–west) distance

53
Q

dx/dt is positive for motions toward the…..

A

east

54
Q

dy/dt indicates

A

meridional (north - south)

55
Q

dz/dt indicates

A

vertical components

56
Q

omega is

A

the vertical motion in isobaric coordinates

57
Q

omega (ω), is defined as

A
58
Q

the following equation represents

A

omega

59
Q

Omega, The pressure-coordinate vertical velocity is ………………….for upward motion

A

negative

60
Q

The pressure-coordinate vertical velocity is negative for upward motion, because

A

pressure decreases with height

61
Q

notations for the 2D horizontal and 3D wind vectors

A
62
Q

the following represents

A

notations for the 2D horizontal and 3D wind vectors

63
Q

the following equations indicate the

A

direction

64
Q

Coriolis parameter is related to

A

the projection of the earth’s rotation onto the vertical (kˆ) axis

65
Q

coriolis parameter is given by

A

f = 2Ωsin ϕ

66
Q

the following is the

f = 2Ωsin ϕ

A

corriolis parameter

67
Q

corriolis is ……. over the equator

A

zero

68
Q

explain each term in the “corriolis parameter”

A

latitude is denoted ϕ and Ω is the earth’s rate of angular rotation, 2π radians day–1, with a day here being the sidereal day (23 h 56 min).

The numerical value of Ω is 7.292x10−5 rads−1.

69
Q

basic variables include

A

pressure (p), temperature (T), density (ρ), and specific volume (α= 1/ρ​ ).

70
Q

density is defined as

A

the mass of air m per unit volume, a cubic meter

71
Q

dewpoint (Td) is the

A

Measures of absolute water vapor content

72
Q

specific humidity (q), and mixing ratio (r) are similar in

A

magnitude

73
Q

specific humidity (q) is the

A

mass of vapor per unit mass (kg) of air mv/m

74
Q

mixing ratio is given by

A

the mass of vapor per unit mass of dry air, mv/md.

75
Q

Values of the mixing ratio and specific humidity can be defined for

A

saturated conditions

76
Q

relative humidity is

A

A measure of the degree of saturation

77
Q

Unless otherwise stated, the units to be used in this text are those of the System Internationale (SI), which is summarized in Table 1.2. The only frequent exception in this text is

A
  • millibar (mb), equivalent to the hectopascal (hPa, or 100 Pa)
  • degrees Celsius (°C), which are equivalent in size to kelvins (K)
78
Q

Quantity: length

Unit:

SI unit and notation:

A

Meter

m

79
Q

Quantitiy: time

Unit:

SI unit and notation:

A

second

s

80
Q

Quantitiy: Mass

Unit:

SI unit and notation:

A

Kilogram

kg

81
Q

Quantity: Temperature

Unit:

Si units and notation:

A

Kelvin

K

82
Q

Quantity: Velocity

Unit:

SI units and notation:

A

Meter/second

m/s

83
Q

Quantity: force

Unit:

SI units and notation:

A

Newoton

N (kg m/s2)

84
Q

Pressure

Unit:

SI unit and notation:

A

(force/area)

pascal

Pa (Nm2 or kg/m s)

85
Q

energy or work

unit:

SI units and notation

A

Joule

J(Nm or kg m2/s2​)

86
Q

the ideal gas law is also known as

A

equation of state

87
Q

the ideal gas law

A

provides a useful relation between the pressure, temperature, and density

88
Q

The ideal gas law equation

A
89
Q

the following equation is for

A

ideal gas law

90
Q

explain each term in the equation

A

Rd is the dry-air gas constant

Tv is the virtual temperature ( The temperature that a parcel of dry air would have if it were at the same pressure and had the same density as moist air. )
Tv= T (1+0.61q). Rd = 287 J/ kg.K.

91
Q

The momentum equations in Cartesian form

A

Synoptic Meteorology (12 decks)

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