PeN-model
"PeN-model"is
the acronym for a numerical model of the atmosphere that was developed
at IMAU (Utrecht University) for education purposes for the courses,
Dynamical Meteorology, Boundary Layers, Transport and Mixing and Simulation
of Oceans, Atmospheres and Climate. Pe stands for "primitive
equations" and N stands for N layers. A 3D version of the model
with N=36 and a 2D version of the model with N=200 are "operational".
The 3D version is used to study the life cycles of baroclinic waves
(cyclones and anticyclones) in middle latitudes (link),
while the 2D version is used to study the interaction between adiabatic
dynamics and diabatic processes, such as absorption and emission of
radiation and latent heat release, in the General Circulation. This
version can be used to understand the subtropical jet, the Hadley
circulation and the polar winter stratospheric vortex, the seasonal
stratospheric zonal wind reversals and tropical cold point at 100
hPa. The latter feature is manifest in panel 1 as an upward bulge
of the 370 K isentrope. The 2D version of the model includes parametrizations
of planetary wave drag and the water cycle. The atmosphere contains
one well-mixed greenhouse gas as a proxy for CO2 and another greenhouse
gas whose density varies exponentially with height (scale height =
2.1 km). The latter greenhouse gas represents water vapour. The water
cycle includes the effects on the energy balance of surface evaporation
and latent heat release in clouds. Clouds do not interact with radiation.
This rather drastic approximation is justified a postriori by the
succes of the model in reproducing the above-mentioned features of
the zonal mean general circulation. The water cycle and planetary
wave drag can easily be switched on or off. On this page two simulations
with the 2D model are described.
2D-SIMULATION OF
THE ZONAL MEAN STATE OF THE ATMOSPHERE: zero obliquity
Several simulations
with the 2D version of the model were performed with zero obliquity,
referred to as "permanent equinox simulations". Run 1f represents
a permanent equinox simulation which includes all the important physical
processes, except absorption of Solar radiation by ozone. It includes
dry convective adjustment, planetary wave drag and water cycle. The
most important elements of the water cycle are evaporation, which
is largest in the (sub)tropics, and condensation, which is largest
over the Inter Tropical Convergence Zone (ITCZ). Panel 2 on the right
shows the zonal wind (black contours, labeled in units of m/s), the
potential temperature (red, cyan and blue lines, labeled in units
of K) and the dynamical tropopause (green, labeled in PVU) after 730
days (2 years) of simulation. At t=0 the atmosphere is isothermal
(T=290 K) and in rest. Wave drag is imposed only if the zonal wind
is eastward both locally and at all levels below. This is based on
the theoretical idea that planetary waves cannot propagate upward
through the atmosphere if the wind is westward. Within the dotted
lines the westward force per unit mass, due wave-drag, is greater
than 0.0025 m/s^2. Blue lines indicate "Underworld" isentropes.
Cyan lines indicate "Middleworld" isentropes. Red lines
indicate "Overworld" isentropes. This terminology was introduced
by N. Shaw in 1931and refined by B. Hoskins in 1991 (pdf).
Middleworld isentropes intersect the dynamical tropopause. The Middleworld
is a very important layer in the atmosphere, because it contains the
subtropical jets. It is also the layer where the stratosphere (in
the extratropics) stands in adiabatic contact with the troposphere
(in the tropics). It contains more mass per square metre in the tropics
than in the extratropics. This is due to the interaction of latent
heat release in the ITCZ and the exponential decay with height of
the isentropic density imposed by radiation. The atmosphere is close
to a steady state after 2 years. Subtropical jets have formed, with
a maximum wind speed of 27 m/s at 250 hPa and ±25° latitude.
The stratospheric polar night jet, centred at ±65° latitude,
is formed much more slowly than the subtropical jets, which are connected
to the Hadly circulation. This circulation is driven mainly by latent
heat release between 900 hPa and 200 hPa above the ITCZ at the equator.
Panel 3 shows the
cross-isentropic flow and the potential vorticity, both in the reference
state of rest (thin green lines) and in the actual state (thick green
line). The dynamical tropopause corresponds to the lowest thick green
isopleth of PV, labeled ±2 PVU. Lines of equal pressure are
indicated by the dotted black lines, labeled in hPa. Cross-isentropic
flow is upward (red contours) in the tropics and downward (blue contours)
in the extratropics, in agreement with reality. You can watch the
corresponding animation by clicking on the icon "Run1f"
(or m4v format"Run1f"
for ipad).
2D-SIMULATION OF
THE ZONAL MEAN STATE OF THE ATMOSPHERE: seasonal cycle
Panels 4 and 5 display
output of the "best" simulation of the zonal mean state
of the atmosphere, including its seasonal cycle. The obliquity is
set to 23.45°. Again, the model is initialized with an isothermal
(290 K) atmosphere in rest. A realistic simulation is obtained only
if wave drag is included in the model. The third panel indicates that
the winter subtropical jet at 20°N-30°N is stronger than the
summer subtropical jet (at 30°S), in agreement with observations.
The tropopause is approximately at the right height. The upward bulge
of the 370 K isentrope in the tropics, which is also seen in the observations
(panel 1) and in run 1f, is an indication of the presence of a tropical
cold layer at about 100 hPa. You
can watch the corresponding animation by clicking on the icon "Run4a"
(or m4v format"Run4a"
for ipad).
Panel 5 shows the cross-isentropic
flow on January 1 of year 3 of the same simulation, as a function
of latitude and potential temperature. Lines of equal pressure are
indicated by the dotted black lines, labeled in hPa. Cross-isentropic
flow is upward (red contours) in the tropics and downward (blue contours)
in the extratropics, in agreement with reality. This is not a trivial
matter. If only radiation were to determine the cross-isentropic or
diabatic circulation, this circulation would consist of only one cell:
upward in the summer hemisphere and downward in the winter hemisphere.
Radiation flux divergence and the diabatic circulation together determine
the vertical position of the dynamical tropopause, which is defined
as the ±2 PVU isopleth of the potential vorticity (the lower
thick green contour).
CONCLUSION ON 2D-SIMULATIONS
The 2D version of the
PeN model reproduces many realistic characteristics of the zonal mean
general circulation of the atmosphere. This can be verified by watching
the movies, which show how the model state, shown in the figures,
is reached, after the model is initialized with an isothermal atmosphere
(290 K) in rest on January 1 of year 1.
A paper on this topic
will be published in Tellus in December 2014 (see publications).
Here is the pdf of a seminar held at Reading University on 10 November
2014: pdf
Results of baroclinic
life cycle experiments with the 3D version of the PeN model are described
in chapter 10 of the lecture notes on Atmospheric Dynamics: link
, and on the following web page: link.