Temperature Lapse rate- decrease of temperature with height:

Temperature  Lapse rate- decrease of temperature with height:

Temperature Lapse rate- decrease of temperature with height: = - dT/dz Environmental lapse rate () order 6C/km in free atmosphere d- dry adiabatic lapse rate- rate at which an unsaturated parcel cools when lifted= 9.8 C/km s- saturated adiabatic lapse rate- rate at which a saturated parcel cools when lifted= 4-9.8 C/km

Stability Vertical momentum equation vertical accelerations due to imbalance between downward directed gravitational force and upward directed pressure gradient force Stable- adiabatic parcel displaced from original altitude accelerated back towards original altitude

Neutral- adiabatic parcel displaced from original altitude. continues to move at a constant speed Unstable- adiabatic parcel displaced from original altitude continues to accelerate away from original altitude Stability Absolutely Stable: d Absolutely Unstable: d

Conditionally Unstable: s < d Lapse Rate Whiteman (2000) Parcel Theory Whiteman (2000)

Skew-T log P diagrams Plot vertical profile of temperature, moisture, wind as a function of elevation Skewed to draw attention to vertical variations in temperature that deviate from typical 6C/km decrease with height Dew point temperature- absolute measure of water vapor = f(e)

Stability Adiabatic parcel conserves potential temperature as it rises or sinks Stable atmosphere: d /dz >0 Neutral atmosphere: d /dz =0

Unstable atmosphere d /dz < 0 Stable atm z

Planetary Boundary Layer PBL-Layer in atmosphere affected by interaction with the surface Free atmosphere- atmospheric layer above the PBL in which state variables largely unaffected by the surface PBL

Daytime convective boundary layer Neutral lapse rate above surface Parcels move freely vertically Strong mixing

Can be several thousand meters deep over western U.S. Nocturnal stable layer Temperature usually increases with height away from the surface inversion Parcels flow horizontally Little mixing Usually few hundred meters deep

Diurnal PBL Evolution Whiteman (2000) Diurnal Change in Temperature Whiteman (2000) Surface based temperature

inversion Whiteman (2000) Elevated Inversion Whiteman (2000) Diurnal changes in stability

Whiteman (2000) Mountain/Valley PBL Whiteman(2000) Mountain PBL

Barry (1992) Free Air vs. Mountain Barry (1992) Valley vs. Summit Barry (1992)

Influence of Wind Speed Barry (1992) Influence of cloud cover Barry (1992)

Diurnal Temperature Range Barry (1992) Diurnal Temperature Range: Western U.S. A. Reinecke Wind Speed

Terrain controls wind speed and direction However, some general characteristics of wind speed vs. altitude Mid-latitudes: Wind speed increases with height Mt. Washington 1915 m: 23m/s in winter;12m/s in summer averages Tropics

Wind speed decreases with height New Guinea 4250 m: 2 m/s DJF average El Misti Peru 4760 m 5 m/s average Wind Speed over Summit Vertical compression of airflow over mountain accelerates air Friction retards flow Small scale roughness effects (<10 m

dimension) Form drag (10m

constriction: Bernoulli effect Conservation of energy: Kinetic Energy + work down by pressure force + potential energy = 0

Vertical compression (U22 U12)/2 + (p2 p1)/ + g(z2 z1) = 0 1 2 U2 > U1 z2 = z1 so

p2 < p1 Lower pressure in constriction Vertical compression (U22 U12)/2 + (p2 p1)/ + g(z2 z1) = 0 2 1

U2 > U1 z2 = z1 so p2 < p1 Lower pressure over summit Wind over Hill

Barry 1992 Free Air vs. Summit Wind speed less at the summit than in the nearby free air Barry (1992)

Roughness Effects For well-mixed conditions (near neutral lapse rate) U2 = u1 ln (z2/zo)/ln(z1/z0) Roughness length zo=.5 h A/S where h height of obstacle, A- silhouette area, S surface area A/S< .1 Zo- height where wind approaches 0

Terrain Roughness Zo (m) Classification Description .0002

Very smooth Water,pavement .03 open Prairie or farm

.25 Rough High crops .5

Very rough Scattered bldgs/ orchards >2 Chaotic


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