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Physical Oceanography > Quiz 2 > Flashcards

Quiz 2 Flashcards

1
Q

physical properties of interest

A

temperature, salinity, density

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2
Q

chemical properties of interest

A

oxygen, nutrients, carbon

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3
Q

conservative sw properties

A

altered only by physical processes: -precipitation and evaporation

  • freezing and thawing
  • mixing
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4
Q

non-conservative sw properties

A

altered by biological activities:

  • respiration/photosynthesis
  • excretion (waster -> nutrients)
  • recycling (nutrients)
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5
Q

greatest seasonal variation at _____ latitudes

A

mid

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6
Q

in the vertical temperature distribution the mixed layer makes up?

A

roughly 2% (uniform temperature)

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7
Q

in the vertical temperature distribution the thermocline makes up?

A

roughly 18 % (rapidly changing temperature)

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8
Q

in the vertical temperature distribution in the deep water?

A

Roughly 80 % (slowly changing temperature)

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9
Q

equatorial ocean has a ___ thermocline

A

shallow

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10
Q

temperate ocean has a ____ thermocline

A

deeper

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11
Q

deep (>1000m) ocean temperatures are_____

A

the same globally

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12
Q

mid-latitude water column may show two thermoclines

A
  1. shallower seasonal

2. deeper permanent

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13
Q

how are seasonal thermoclines developed?

A
  1. surface cooling and higher winter wind generates deep mixing, increases cooling of the surface ocean
  2. summer decreased wind and higher heating warms surface
  3. this process lead to formation of permanent thermocline
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14
Q

the mixed layer depth is ___ in the tropics

A

relatively constant

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15
Q

there is seasonally variable in ____ regions

A

subpolar

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16
Q

where is there deep water formation

A

greenland and iceland

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17
Q

where is there deep MLDs?

A

Southern Ocean and North Atlantic

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18
Q

In-situ

A

the temperature we measure (in-place) of a water parcel, at a particular depth (pressure). Not corrected for compressibility (volume change)

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19
Q

Potential Temperature

A

Temperature the water would have if it was brought adibatically to the surface. Corrected for compression

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20
Q

density of seawater is a ___ function of ___,___,___

A
  • nonlinear

- salinity, temperature, pressure

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21
Q

What is the primary factor that is controlling sw density?

A

Temperature

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22
Q

what is the equation of state for seawater?

A

ρ=ρ(S,T,p)

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23
Q

____ is largely determined by temperature

A

Density

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24
Q

factures controlling density

A
  • pressure (largest but often ignored)
  • temperature (most important for circulation)
  • salinity (important for deep water formation)
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25
Q

seawater density

A

1024 kg/m^3

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26
Q

denisty equation

A

σ (density - 1000) = ρ - ρ ref

ρ ref = 1000 kg m^-3

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27
Q

seawater is ____:
volume ___ with increasing pressure
density ___ with increasing pressure

A

slightly compressible
decreases
increases

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28
Q

sigma

density of 1027.25 is what in sigma

A

sigma is density in (kg m^-3) - 1000

1027.25 - 1000 = 27.25

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29
Q

Density and sigma often written like this

A

σ(s,t,p) = (ρ(s,t,p)) - 1000
Where s is salinity
t is temperature
p is pressure

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30
Q

sigma-t equation

A 
sigma(t) (σt
) = σ(s,t,0) = ρ(s,t,0) - 1000
 where ρ(S,T) is
density of a sample of seawater of T and S, at
a standard atmospheric pressure
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31
Q

what is sigma-t useful for

A

mapping water properties along density surfaces, without mixing water flows along these density surfaces

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32
Q

Sigma-theta equation

A

σϴ is σ(s,ϴ,0) = ρ(s,ϴ,0) – 1000

Where ϴ stands for potential temperature

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33
Q

what does sigma-theta consider

A

adiabatic temperature changes relating to processes in which heat does not enter or leave the system concerned

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34
Q

potential temperature (density)

A

potential temperature is used to calculate potential density. potential temperature (density) of a parcel of fluid at pressure is the temperature (density) that parcel would have if brought to a standard reference pressure, usually 1 atmos in a way that no energy was exchanged with the surrounding water (adiabatically)

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35
Q

potential temperature is

A

temp at 1 atm

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36
Q

potential temperature changes are dependent on

A

thermal expansion coefficients for temperature and salinity

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37
Q

sigma theta for deep water is calculated at

A

400 dbar σ4

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38
Q

increasing pressure causes the in-situ temperature to ____ and the in situ density to ___

A
  • increase (adiabatic warming)

- increase

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39
Q

potential density

A

remove effect of pressure on temperature and density. relevant to the dynamics of the circulation

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40
Q

as temperature increases density ____

A

decreases

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41
Q

as salinity increases density ____

A

increases

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42
Q

General characteristics of salinity distribution

A
  • surface salinity variable
  • deep water generally high salinity
  • minimum: temperate & intermediate-depth
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43
Q

surface salinity pattern

A

strong meridional (n-s) patterns

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44
Q

regional differences in salinity

A

Highest in N. Atlantic

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45
Q

salinity range in the majority of the ocean

A

34-35 ppt

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46
Q

temperature range of the majority of the ocean

A

0-5degC

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47
Q

gases are more soluble in ___ water

A

colder

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48
Q

02 concentration in surface water mostly dependent upon temperature _____

A

saturation

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49
Q

oxygen distribution mid water minimum

A
  • relatively rapid respiration

- no gas exchange with atmosphere

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50
Q

oxygen distribution deep water

A

well-oxygenated

  • no gas exchange with atmosphere
  • supplied from high latitude
  • very slow respiration
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51
Q

oxygen minimum zones

A

< 0.2 ml o2/liter

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52
Q

where is co2 enriched

A

the deep sea via biological pump and higher solubility

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53
Q

where is the greatest concentration of carbon

A

north pacific

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54
Q

how to “age” water

A
  • rates of non-conservative properties changes: production of nitrate and consumption of 02
  • tracers (bomb tritium and CFCs)
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55
Q

hyrdographic parameters

A

temperature, salinity and pressure

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56
Q

temperature and salinity of interest in themselves : define

A

water masses

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57
Q

CTD

A

used for hydrographic work , conductivity, temperature and depth (pressure)

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58
Q

salinity

A

total dissolved g of slats in a kg solution (ppt)

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59
Q

major seawater chemistry is dominated by

A

Na and Cl

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60
Q

salinity equation

A

S=(mass of dissolved compounds kg)/(mass of seawater kg) x 1000
units: parts per thousand

61
Q

salinity is based on _____ assuming the _____

A

chlorinity, law of constant proportions

62
Q

chlorinity

A

grams of Cl- per kilogram of seawater

Salinity (‰) = 1.80655 * Clorinity (‰)

63
Q

psu

A

practical salinity unit

64
Q

absolute salinity

A

SA = (35.16504 g kg−1/ 35) *SP
+ δSA
(lat,long,p)

SP
is PSU
δSA as a function of latitude, longitude & pressure

65
Q

current salinity measurements are based on

A

conductivity measurements matched to seawater samples where chlorinity measured and Marcet’s principle assumed

66
Q

measuring pressue

A

least precise of CTD measurements

pressure in decibars (dbar = ~1m)

67
Q

role of atmosphere/ocean interactions

A
  • forcing of wind-driven ocean circulation
  • energy transfer (wind stress)
  • albedo and thermal inertia
  • heat budget
  • radiative equilibrium temperature
68
Q

ocean-atmosphere interactions

A
  • wind stress (energy transfer)
  • atmosphere cools ocean (evaporation)
  • ocean cools/warms atmosphere
69
Q

evaporation ___ the ocean/ ___ the air

A

cools

warms

70
Q

precipitation ___ the air / ___ the ocean

A

cools

warms

71
Q

mechanisms for air-sea interactions:

Heat exchange and water exchange

A
  1. Radiation (wavelength dependent)
  2. evaporative (exchange of latent heat)
  3. Precipitation (exchange of latent heat)
  4. conduction (heat exchange by molecules)
72
Q

air-sea interaction momentum exchange

A

friction via wind

73
Q

rediation

A

heating from solar radiation (IR spectrum)

74
Q

flux equation

A

items/area*time

75
Q

unit of force

A

newton N (kg m sec-2)

76
Q

unit of work

A

joule N * m (kg m2 sec-2)

77
Q

unit of power

A

watt J sec-1

kg m2 sec-3

78
Q

power equation

A

power = force x velocity

79
Q

solar heat flux

A

342 watts/m^2
(at the top of the atmosphere)
drives wind and photosynthesis

80
Q

geothermal heat flux

A

0.0075 watts/m^2 (at Earth surface, bottom of the atmosphere) drives plate tectonics: oceanic ridges

81
Q

solar / geothermal flux ratio

A

~3200

82
Q

concept of black body radiation :

A

all objects emit
electromagnetic energy (per unit surface area
and time) proportional to their temperature

83
Q

Thermal radiation equation

A 
Stephan-Boltzman (S-B) relationship
Watts / m2 = E = σ * e * k4
σ = S-B constant 5.67 10-8 W m-2 k
-4
e = emissivity = 1 in ideal case
k4 = Kelvin temperature to fourth power
84
Q

thermal radiation wein’s displacement law

A

as temp increases

  • total energy increases by the power of 4
  • peak energy shifts to higher frequency (smaller wavelength)
85
Q

what is the S-B constant

A

5.67 10-8 W m-2 k

86
Q

what are the three key EM spectrum bands

A
  1. ultraviolet
  2. visible
  3. infrared radiation
87
Q

ultraviolet radiation

A

radiation within band with wavelength from 1 to 400 nm. UV radiation is present in sunlight, and contributes about 10% of electromagnetic radiation output from the sun

88
Q

visible light

A

light occurs within the a band rnaging from 400-700 nm

89
Q

infrared radiation

A

within band ranging from 700-100,000 nm. IR is not visible EM energy, but is heat

90
Q

is solar radiation constant

A

seasonality due to earth’s tilt

91
Q

sunspot

A

a cooler and darker, region of the sun’s surface caused by solar magnetic disturbance

92
Q

solar flare

A

a violent eruption of plasma from the sun, whipped up by intense magnetic activity

93
Q

what are milankovitch cycles

A

cyclical movment related to the Earth’s orbit around Sun.

There are 3: eccentricity, axial tilt and precession

94
Q

what are the three types of milankovitch cycles

A

eccentricity, axial tilt, and precession

95
Q

eccentricity

A

earth encounters more variation in the energy that is receives from the sun when Earth’s orbit is elongated than it does when earth’s orbit is more circular
3 cycles of periods; 96,125,400 K years
affects variability in solar energy reaching Earth’s surface

96
Q

Tilt (obliquity)

A

the tilt of Earth’s axis varies between 22.2 and 24.5 degrees. The greater the tilt angle is, the more solar energy the poles receive.
a cycle of perido: 41 K years
affects variability in solar energy reaching Earth’s surface

97
Q

precession

A

a gradual change, or “wobble,” in the orientation of Earth’s axis affects the relationship between Earth’s tilt and eccentricity.
3 cycles of periods: 12, 22, 24 k years
affects relationship of tilt and eccentricity

98
Q

on average, Earth and atmosphere reflects about

A

~30% of incoming radiation

99
Q

reflectivity

A

proportion of the energy that “bounces off” versus being absorbed

100
Q

troposphere

A

<10% height 90% of mass of atmosphere

  • inherently unstable
  • weather (mixing)
101
Q

1st law of thermodynamics equation

A

heath change = internal energy + work done

102
Q

adiabatic expansion

A

work done without heat loss or gain, so internal temperature changes

103
Q

Adiabatic Expansion

A

∂T/∂Z = -g / Cp
(Note: Z is elevation)
– g = gravitational acceleration on earth surface
(~9.81 m sec-2)
– Cp = specific heat (dry air = 1000.35 J kg-1 k
-1)
• This works out to be ~ 9.8 K km-1
(sign dependent on sign of pressure change)
Higher pressure -> Higher Temperature (+)
Lower pressure -> Lower Temperature (-)

104
Q

Lapse rate

A

∂T/∂Z of air an parcel
(water parcels vary in composition)
– Moist air lapse rate = -6.5 K km-1
– Dry air lapse rate = -9.8 oK km-1

105
Q

Lapse Rate why

A
  • dry air cools as pressure decreases: -9.8 K km^-1
  • lapse rate decreases with increasing H20 content due to latent heath release
  • as water vapor condenses, it releases heath … which counteracts the parcel’s cooling
106
Q

centigrade to kelvin

A

centigrade - 273 = Kelvin

107
Q

temperature decline with altitude in Troposphere caused by

A

adiabatic cooling
-typical lapse rate (wet air) ~ 6.5 degree C/km
-adiabatic cooling (dry air) rate 9.8 C /km
~3.3 C/ km increase in potential temperature

108
Q

is the stratosphere stable?

A

strongly dense, therefore stable

109
Q

is the troposphere stable?

A

No, very weakly density stratified therefore turbulent mixing (weather)

110
Q

mean earth temp

A

15 C or 288 K

111
Q

Global Heath Budget (Energy transfer processes)

A
  • solar radiation (+)
  • geothermal heat (minor ~0.03% of solar input) (+)

– Long wave radiation to space (-)
– Conductive heat loss (-)
– Latent heat loss (-)

112
Q

Earth average albedo 30%

A
  • 20% absorbed the atmosphere
  • 50% absorbed by the Earth
  • 5% IR directly to space
  • 25 of 50 units from Earth are absorbed by the Atmosphere and are then reradiated to space (greenhouse effect)
  • most latent heat is found in water vapor
113
Q

sensible heat

A

at most temperatures, adding heat to water produces a proportional temperature rise

114
Q

sensible heat leads to a __ in temperature. Latent heat ____ to a rise in temperaure

A

rise, does not lead

115
Q

what equation do you use to calculate the average earth temperature

A

stephan-boltzmann equation

116
Q

equation for heat radiated from earth’s surface

A

(4πR2) * (σ * e * k
4) (σ = constant)
(Remember: e = 1)
(k = temp. in kelvin r=radius

117
Q

radiative equilibrium temperature

A

255 K (-18C), with this temperature the Earth radiation will be centered at 11μm, within IR range

118
Q

average surface temperature of earth

A

15 C

119
Q

why is there a temperature discrepancy between the average surface temperature and radiative equilibrium temperature

A

difference because Earth not true black body

120
Q

the global heat budget vary with

A

location (latitude) and earth surface characteristics (albedo)

121
Q

the greenhouse effect*

A

the process by which radiation from a planet’s atmosphere warms the planet’s surface to a temperature above what it would be without its atmosphere

trapping of the sun’s warmth in a planet’s lower atmosphere, due to the greater transparency of the atmosphere to visible radiation from the sun than to infrared radiation emitted from the planet’s surface

122
Q

what are the main gases that absorb and trap IR radiation in the atmosphere

A

water vapor (36-72%), carbon dioxide (9-26%), Methane (4-9%) and Ozone (3-7%)

123
Q

earths average temperature

A

5.12 C

124
Q

what two parameters are used to measure sea water salinity

A

conductivity or chlorinity

125
Q

incoming solar radiation

A

+324 Wm^-2

126
Q

incoming solar radiation absorbed by the atmosphere

A

+67 Wm^-2

127
Q

incoming solar radiation absorbed by Earth’s surface

A

+168 Wm^-2

128
Q

incoming solar radiation total reflected solar radiation

A

-107 Wm^-2

129
Q

incoming solar radiation reflected by clouds, aerosols and atmospheric gases

A

-77 Wm^-2

130
Q

incoming solar radiation reflected by the Earth’s surface

A

-30 Wm^-2

131
Q

total outgoing longwave radiation

A

-235 Wm^-2

132
Q

Long wave radiation emitted by the Earth’s surface

A

-390 Wm^-2

133
Q

Back longwave radiation reabsorbed by the Earth’s surface

A

+324 Wm^-2

134
Q

Latent heat from Earth’s surface

A

-78 Wm^-2

135
Q

albedo*

A

the proportion of the incident light (radiation) that is reflected by a surface, rather than being absorbed. Values are expressed as proportions of the total incident light (or radiation)

136
Q

latent heat*

A

latent head is energy released or absorbed by a thermodynamic system during a constant-temperature process (usually a phase transition). Latent heat can be understood as energy in hidden form, which is supplied or extracted to change the state of a substance without changing its temperature

137
Q

sensible heat*

A

sensible head is heat exchanged by a thermodynamic system that changes the temperature of the system. As the name implies, sensible heat is the heat that you can feel. The sensible heat possessed by an object is evidenced by its temperature

138
Q

conservative property*

A

a water property not affected by biology (temperature and salinity)

139
Q

albedo values from low to high

A

ocean, forest, grasslands, soil, desert, ice, fresh snow

140
Q

ocean heat flux input

A

solar flux

141
Q

ocean heat flux output

A

latent heat, long wave radiation, sensible heat (conduction)

142
Q

ocean contains ___ times more heat than the atmosphere and about ___ times than the land

A

1000, 100

143
Q

Heat capacity of the ocean, lithosphere and atmoshphere

A

4000 J/kg
800 J/kg
1000 J/kg

144
Q

exchange volume for ocean in global heat budget

A

ocean: upper 10-100 m
lithosphere: 1-2m
troposphere: 10 km

145
Q

conservation of heat energy in the global ocean

A 
Qt = Qsw + Qlw + Qs + Ql
\+ Qv
• Oceanic heat sources / sinks (from Stewart)
– Solar radiation: Qsw (+)
– Long wave radiation: Qlw (-)
– Conductive (sensible) heat Qs (-)
– Latent heat loss Ql (-)
– Advective heat loss/gain Qv (+/-)
146
Q

long wave flux strongly influenced by:

A
  • cloud cover amount and height

- atmospheric water vapor content

147
Q

mid-depth salinity is the result of what

A

colder, lower salinity waters from regions of excess rain sinking to depth (thermohaline circulation)

148
Q

ϴ

A

potential temperature.

Physical Oceanography (3 decks)

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