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Lecture 6 • Atmospheric Pressure

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Lecture 6 • Atmospheric Pressure ATMOS 5130 Lecture 6 • Atmospheric Pressure • Pressure Profiles for Idealized Atmosphere Goal • Understand how temperature, pressure and altitude are related in the atmosphere. Recall from last lecture Hypsometric �&�( �- Δ� = ln Equation � �. Allow for calculation of pressure at any height Pressure Profiles for Idealized Atmosphere • Constant Density Atmosphere • Unrealistic • Better representation of the ocean • Atmosphere had the same mass as now, but had a constant density it would be only 8.3 km deep :1 ≈ −�� Hydrostatic Equation :8 1(3) 8 / �� = −�� / �� 15 9 � � = �9 − ��� Pressure decreases linearly with height Pressure Profiles for Idealized Atmosphere • Constant Density Atmosphere � � = �9 − ��� • Pressure is decreasing with height • Density is constant • SO, Temperature must decease with height � = ��&� IDEAL GAS LAW �� �� = �� Differentiate with respect to elevation �� & �� �� Substitute in Hydrostatic Equation = −�� �� := > = − = -34.1 C/km :8 ?@ Constant Density Atmosphere � � = �9 − ��� Autoconvective Lapse Rate := > = − = -34.1 C/km = ΓBCDE :8 ?@ �ℎ��: Γ > ΓBCDE Density above greater than below! Density Inversion => Creates a mirage Above a very hot road, a layer of warm air whose density is lower than air above. The denser air slows light very slightly more than the less dense layer. So, one sees sky where the road should be, we often interpret this as a reflection caused by water on the road Pressure Profiles for Idealized Atmosphere Constant Density Pressure Profiles for Idealized Atmosphere • Isothermal Atmosphere &1 = −�� Hydrostatic Equation &8 Again substitute in the ideal gas law, �� �� = −�� = − �� �&� Solve � 1 � � � = � exP − �� = − �� 9 � � �&� Where: 1 1 � 8 / �� = − / �� � � � � � 15 & 9 � = & 9 � �� � ln = − �9 �&� Scale Height Constant Density Atmosphere � � = � − ��� 9 Approximate scale heights for selected Solar System bodies Venus: 15.9 km Scale Height (H): solve for z, when p(z) = 0, Earth: 8.3 km Mars: 11.1 km � Jupiter: 27 km � = 9 �� Saturn: 59.5 km Titan: 40 km Uranus: 27.7 km substitute the Ideal Gas Law Neptune: 19.1–20.3 km Pluto: ~60 km � � � = & 9 � In other words: scale height is the increase in altitude for which the atmospheric pressure decreases by a factor of e-1 or about 37% of its original value. Pressure Profiles for Idealized Atmosphere • Constant Lapse Rate atmosphere � = �9 − Γ� • Normally Γ >0, temperature decreases with altitude • When Γ >0, temperature increases with altitude • INVERSION Pressure Profiles for Idealized Atmosphere • Constant Lapse Rate atmosphere � = �9 − Γ� Take the hydrostatic equation and combine with Ideal Gas Law �� �� = −�� = − �� �&(�9−Γ�) 1 � �� �� = − � �& �9 − Γ� 1 1 � 8 �� / �� = − / � � � − Γ� 15 & 9 9 � � � − Γ� ln = ln − 9 �9 �&Γ �9 > �9 − Γ� ?@Q �(�) = �9 �9 Pressure Profiles for Idealized Atmosphere • Constant Lapse Rate atmosphere � = �9 − Γ� Take the hydrostatic equation and combine with Ideal Gas Law �� �� = −�� = − �� �&(�9−Γ�) 1 � �� �� = − � �& �9 − Γ� 1 1 � 8 �� / �� = − / � � � − Γ� 15 & 9 9 � � � − Γ� ln = ln − 9 �9 �&Γ �9 �(�) > �9 − Γ� ?@Q �(�) = �9 �9 Pressure Profiles for Idealized Atmosphere • Constant Lapse rate atmosphere > �(�) ?@Q �(�) = �9 �9 Valid for Γ < 0 Exponent of the ratio is negative, so pressure still decreases with height > is ratio of autoconvective to actual lapse rate ?@Q So, what happens if � = ����� ? Pressure Profiles for Idealized Atmosphere • Constant Lapse rate atmosphere > �(�) ?@Q �(�) = �9 �9 Valid for Γ < 0 Exponent of the ratio is negative, so pressure still decreases with height > is ratio of autoconvective to actual lapse rate ?@Q So, what happens if � = ����� ? =(8) �(�) = �9 - Pressure is linear function of z =5 Temperature vs. Altitude 20 Γ=0 15 Γ =6.5 K/km z [km] 10 Γ=Γ 5 auto 0 0 100 200 300 T [K] Density vs. Altitude 20 Γ = 0 ; Isothermal 15Γ = 6.5 K/km; Constant Lapse Rate Γ = Γauto; Autoconvective; Constant Density = g/Rd Γ=6.5 K/km z [km] 10 5 Γ=0 Γ=Γauto 0 Fig. 4.4 0.0 0.2 0.4 0.6 0.8 1.0 1.2 1.4 ρ (kg/m3) Pressure vs. Altitude 20 15 Γ=0 Γ=6.5 K/km z [km] 10 5 Γ=Γauto 0 0 200 400 600 800 1000 1200 p [hPa] Temperature vs. Altitude 20 Γ=0 15 Γ =6.5 K/km z [km] 10 Γ=Γ 5 auto 0 0 100 200 300 T [K] Density vs. Altitude 20 15 Γ=6.5 K/km z [km] 10 5 Γ=0 Γ=Γauto 0 0.0 0.2 0.4 0.6 0.8 1.0 1.2 1.4 ρ (kg/m3) Pressure vs. Altitude 20 15 Γ=0 Γ=6.5 K/km z [km] 10 Isothermal 5 � Γ=Γauto � � = � exP − 9 � 0 0 200 400 600 800 1000 1200 p [hPa] Constant Lapse Rate Γ = 0 ; Isothermal > �(�) ?@Q Γ = 6.5 K/km; Constant Lapse Rate �(�) = �9 �9 Γ = Γauto; Autoconvective Constant Density Autoconvective � � = �9 − ��� Fig. 4.4 Temperature vs. Altitude 20 Γ=0 15 Γ =6.5 K/km z [km] 10 Γ=Γ 5 auto 0 0 100 200 300 T [K] Density vs. Altitude 20 15 Γ=6.5 K/km z [km] 10 5 Γ=0 Γ=Γauto 0 0.0 0.2 0.4 0.6 0.8 1.0 1.2 1.4 ρ (kg/m3) Pressure vs. Altitude 20 Γ = 0 ; Isothermal 15 Γ=0 Γ = 6.5 K/km; Constant Lapse RateΓ=6.5 K/km Γ = Γauto; Autoconvective Constant Density z [km] 10 5 Γ=Γauto 0 0 200 400 600 800 1000 1200 Fig. 4.4 p [hPa] Piecewise Linear Temperature Profile • Ultimate Approximation is model based on series of stacked layers • Each layer exhibits a different constant lapse rate • Generally speaking, if a layer is thin enough, then all the above methods give you about the same result. > �YZ- ?@Q[ �YZ- = �Y �Y Piecewise Linear Profiles Three Layers 24 Layers 10 10 20 20 30 30 50 50 70 70 100 100 [hPa] 150 [hPa] 150 200 200 250 250 300 300 Pressure Pressure 400 400 500 500 700 700 850 850 925 925 1000 1000 -90 -80 -70 -60 -50 -40 -30 -20 -10 0 10 20 30 40 -90 -80 -70 -60 -50 -40 -30 -20 -10 0 10 20 30 40 ! ! Temperature [ C] Temperature [ C] Fig. 4.5.
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