LECTURE 3

 

METO/CHEM 637

 

ATMOSPHERIC CHEMISTRY

 

RUSSELL R. DICKERSON

 

NOTES

 

1.      HW#1 due Thrs

2.      HW#2 data in excel

3.      ISSUES with Chameides and Walker (1973) paper

Is CH4 oxidation the major source of CO?

Do steady state calculation

Way too much NO and NOx for a global average; 3 ppb this is a suburban valve

RO2 + NO -> NO2 + RO is important.

 

 

 

 

 

 

 

 

Finlayson-Pitts

Seinfeld CH. 1 & some of 16

Wayne Chapt. 5,9

 

OUTLINE

ID. BIOGEOCHEMICAL CYCLES AND ATMOSPHERIC BUDGETS

EXAMPLES

1. WATER

2. CARBON

3. OXYGEN

II. THERMODYNAMICS

A.            ENTHALPY FORMATION AND COMBUSTION

 

 

ID. Biogeochemical Cycles and Atmospheric Budgets

Definitions:

 

Biogeochemical Cycle -The process by which an element or compound passes through the atmosphere, biosphere, and geosphere (oceans and crust).

 

Global Budget - The total atmospheric burden of a substance and the rates of its production and destruction, or its source and sink strengths.

 

Steady State - The condition of constant concentration of a substance in the atmosphere. Steady state implies that the sources and sinks are equal; the lifetime, τ (also called residence time) is the burden divided by production (or destruction) rate.

 

τ = BURDEN/PROD.

 

After time τ (1 - e-1) of the material has been exchanged. We will derive this later.


 

 

EXAMPLE 1 - WATER

Atmosphere contains 0.48% water on average

        Burden = grams water in the global atmosphere:

0.48 x 0.01 x 18/29 x (5.15x1021) = 1.5x1019 g H2O

(note mass of atmosphere and surface area on table in syllabus)

or

 

1.5x1019/5.13x1018 = 3 g/cm2

 

UNITS: mole fraction x Mwts x mass atmos. = mass water

 

 

        Source - evaporation - rate not easily measured

 

        Sink - precipitation - estimates range from 93 to 120 cm/yr. We will use 100 cm/yr or 100 grams per cm 2 year. The strength of this sink is uncertain because of limited observations over the oceans.

 

Assume steady state, i.e., sources = sinks

 

Lifetime (τ) = 3/100 years or 11 days

 

Does this tell us anything useful about water in the atmosphere?

 

1.         τ << transport time - more H2O in areas of strong sources. The fraction of water in the atmosphere varies from a few percent near the surface to < 10 ppm at the tropopause.

2.         Global budgets are best for compounds whose lifetimes are much longer than the transport time of ca 1 year.

3.         Absolutely absurd approach w.r.t. meteorology - tells us doodley squat about the probability of rain.

4.         A wide variety of units is possible

5.         The longer the lifetime the more stable concentration in time and space.

NOTE: In general, the shorter the τ the higher variation in time and space (Junge, Tellus, 1974).

EXAMPLE 2 - CARBON

(VIEWGRAPH)

 

How much C is there in the atmosphere? We will assume all the carbon is CO2, and that the mean concentration, [CO2], is 350 ppm.

 

        Burden

 

350 x 10-6 x 1.8 x 1020 x 12 = 7.6x 1017 gC (as CO2)

UNITS: [CO2] x moles air x g/mole = gC

 

        Major source - Respiration

 

        Major sink - Photosynthesis

 

But if the biosphere is in S.S. then the net is zero. The biosphere is actually slight source of CO2 to the atmosphere because of forest destruction. Story about Brazil with rainforest and U.N. speech.

 

        Other source - fossil fuels, volcano, oceans

 

        Other sink - oceans

 

 

Lifetime = burden / sources

 

τ = 7.6x1017 over {(1.5 + 0.05 + 0.05 + 0.0007) x 1017} 5 yr

 

Can man make much of a change in the burden?

Total reduced (fossil and living) carbon = 142 x 10 17 g

[CO2] = 142 over 7.6 x 350 ppm = 6500 ppm!

 

Yes, we can make a big increase.

EXAMPLE 3 OXYGEN

{VIEWGRAPH}

Can fossil fuel burning affect atmospheric oxygen?

Where is the oxygen?

 

        Burden:

 

In the atmosphere: 32/29 x 0.21 x 5.15 x 1021 = 1.2x 1021 g O as O2

UNITS: mwt's [O2] x mass atmosphere = grams O2

In the oceans as H2O: (16/18)x(1.6x1024) = 1.4x10 24 g O

UNITS: mwt's x mass seas x mass O in seas

The crust doesn't count, because the exchange is very slow but we can calculate the burden anyway.

 

3 x 106 x 17 x 103 x 5.1 x 1014 x .47 = 1.2 x 1025 g O

UNITS: density x depth x area x O by wt x O in crust

UNITS: g/m3 x m x m2 = g

 

        Biomass: 0.015 x 1021 grams C

 

        Organic sediments: 45 x 1021 grams C

 

 

Take all of organic C and make CO2 out of it you produce:

142x1017 x 32 over 12 = 380 x 1017 g O as CO2

UNITS: mass C X mwt's = mass O2 consumed.

{380x1017} over {1.2 x 1021} = 3.2%

 

 

Problem for students: At what altitude is the oxygen partial pressure reduced by 3.2%?

DPO2 = 3.2%

ans. about 250 m

 

CHEMICAL THERMODYNAMICS

A. ENTHALPY OF FORMATION AND COMBUSTION

(In search of the Criterion of Feasibility)

1. First Law of Thermodynamics (Joule 1843 - 48)

dE = DQ DW

(In METO 620 E = U)

 

The energy of a system is equal to the sum of the heat and the work.

Explain eq. of state and exact differentials

 

1. Define Enthalpy (H)

dH = dE + d(PV)

 

dH = DQ - DW + PdV + VdP

At constant pressure and if the only work is done against the atmosphere i.e. PdV work, then

DW = PdV

 

dHp = DQp

 

and DQ is now an exact differential, that is independent of path.

 

For example, the burning of graphitic carbon might proceed through CO:

DHfo

Cgraph. + O2 CO2 -94.0 kcal/mole

Cgraph + 1/2 O2 CO -26.4

CO + 1/2 O2 → CO2 -67.6

------------- ------------------------

NET Cgraph + O2 → CO2 -94.0 kcal/mole

This is Hess' law. There is a table of DHfo in Pitts & Pitts,

Appendix I, p. 1031. The units of kcal are commonly used because DHfo is usually measured with Dewars and change in water temperature.

 

Note that you can do the same thing at constant volume except the result is:

 

DQv = dEv

 

2. Heat capacity:

 

The amount of heat required to produce a one degree change in temp in a given substance.

 

C = DQ/dT

Cp = (∂Q/∂T)p = (∂H/∂T)p

 

Cv = (∂Q/∂T)v = (∂E/∂T)v

 

Because DQp = dH and DQv = dE

 

For an ideal gas PV = nRT

Cp = Cv + R

Where R = 2.0 cal/moleK

 

The heat capacity depends on degrees of freedom

Translation = 1/2 R each

(every gas has 3 translational degrees of freedom)

 

Rotation = 1/2 R

 

Vibration = R

 

For a gas with N atoms you see 3N total degrees of freedom and 3N - 3 internal (rot + vib) degrees of freedom.

 

Equipartition principle: As a gas on warming takes up energy in all its available degrees of freedom.

 

 

 


 

(VIEWGRAPH)

 

Measured Heat Capacities

 

Cv Cp

He 3.0 5.0

 

Ar 3.0 5.0

 

O2 5.0 7.0

 

N2 4.95 6.9

 

CO 5.0 6.9

 

CO2 6.9 9.0

 

SO2 7.3 9.3

 

H2O 6.0 8.0

 

Cv = R/2 x (T.D.F.) + R/2 x (R.D.F.) + R x (V.D.F.)

 

Cp = Cv + R

 

Translational degrees of freedom - always 3.

 

Internal degrees of freedom = 3N - 3

 

Where N is the number of atoms in the molecule

 


 

Check Cv(He): 3 x R/2 = 3.0 cal/(mole K)

 

Cv(O2): 3 x R/2 + 2(R/2) + 1(R) = (7/2) R = 7.0 cal/(mole K)?

 

What's wrong?

 

Not all energy levels are populated at 300 K

 

Not all the degrees of freedom are active (vibration)

 

O2 vibration occurs only with high energy; vacuum uv radiation.

 

at 2000K Cv (O2) approx 7.0 cal/mole K

 

Students: show that on the primordial Earth the dry adiabatic lapse rate was about 12.6 K/km.


 

IIA. ENTHALPY (HEAT)

1. FORMATION

 

Definition: The enthalpy of formation. DHfo is the amount of heat produced or required to form a substance from its elemental constituents.

The standard conditions, represented by a super "o", are a little different from those for the Ideal Gas Law: 25oC (not 0oC), 1.0 atm. and the most stable form of elements. The standard heat of formation is zero for elements. This quantity is very useful for calculating the temperature dependence of equilibrium constants and maximum allowed rate constants. It was thought for a long time that DH was the criterion of feasibility. Although DH tends toward a minimum, it is not the criterion. Things usually tend toward minimum in DH, but not always. Examples are the expansion of a gas into a vacuum, and the mixing of two fluids.

 

 

{VIEWGRAPH}

 

2. ENTHALPY OF REACTIONS

 

The heat of a reaction is the sum of the heats of formation of the products minus the sum of the heats of formation of the reactants.

 

DHrxn = S DHfo(products) - S DHfo(reactants)

 

 

The change of enthalpy of a reaction is fairly independent of temperature.

 

EXAMPLE: ENTHALPY CALCULATION

{VIEWGRAPH}

Which is hotter, an oxygen-acetylene flame or an oxygen-methane flame?

REACTIONS

C2H2 + 2.5O2 → 2CO2 + H2O

 

CH4 + 2O2 → CO2 + 2H2O

 

Note: melting point iron = 1535 C.

 

3. BOND ENERGIES

See Appendix III of Pitts for a table of bond energies. The quantity is actually heat not energy. Don`t confuse with free energy to follow.

 

Definitions:

 

Bond Dissociation Energy - The amount of energy required to break a specific bond in a specific molecule.

 

Bond Energy - The average value for the amount of energy required to break a certain type of bond in a number of species.

 

{VIEWGRAPH}

EXAMPLE: O-H in water

We want

H2O → 2H + O +221 kcal/mole

We add together the two steps:

 

H2O → OH + H +120

OH → O + H +101

---------------------------------

NET +221

 

Bond energy (enthalpy) for the O-H bond is 110.5 kcal/mole, but this is not the b.d.e. for either O-H bond.

 


 

EXAMPLE: C-H bond in methane

 

We want DHfo for the reaction:

CH4 → Cgas + 4H

any path will do (equation of state.)

 

DHfo (kcal/mole)

CH4 + 2 O2 → CO2 + 2H2O -193

CO2 → Cgraph + O2 +94

2H2O → 2 H2 + O2 +116

2H2 → 4H +208

Cgraph → Cgas +171

------------ -----------------------------------

NET CH4 Cgas + 4H + 396 kcal/mole

 

The bond energy for C-H in methane is:

 

+396/4 = +99 kcal/mole

 

Bond energies are very useful for "new" compounds and substances for which b.d.e. can`t be directly measured such as radical.