Meteorology/Everyday Weather

This page refers to the 2010, 2013, and 2016 topic of Meteorology. For sample notesheets for this topic, see Everyday Weather Notes and EpicFailOlympian's Everyday Weather Notes.

General Info
Everday weather is what some would consider the most complex subject for Meteorology, mainly because it covers all bases of Meteorology, even some climate and storm systems. but the major information to learn will  include:
 * Structure and composition of the modern atmosphere
 * Properties of water
 * Types of clouds associated with weather
 * Heat transport including the energy budget, insolation, albedo, convection and radiation
 * Atmospheric circulation including the Coriolis Effect, planetary wind belts, jet stream, local wind patterns (including Chinook winds, mountain and sea breezes) and the three cell model of circulation
 * Air Masses
 * Fronts
 * Surface weather stations
 * Satellite imagery,isobars, isotherms,surface weather maps showing isobars, fronts, and radar data; metograms; Doppler imagery
 * Weather instrumentation including barometers, thermometers, anemometers, sling psychrometers, rain gauges, radiosondes, rawinsondes, and the Beaufort scale
 * Atmospheric phenomena

Everyday Weather focuses on the mechanics of Earth’s atmosphere and how it causes daily weather. This is a large shift from Climate that emphasizes long-term predictable patterns of weather.

The Atmosphere
The sections below illustrate the concepts and importance of the atmosphere in the study of meteorology.

Origins of the Atmosphere
The origin of Earth’s atmosphere is subject to  debate. It is fairly certain that the Earth, when it was formed five billion years ago, was too hot to retain the gasses in its primordial atmosphere. Earth’s first atmosphere most likely consisted of helium, hydrogen, ammonia and methane.

What happened over thousands of years is that volcanoes emitted amounts of water vapor, carbon dioxide and nitrogen - the same gases emitted by volcanoes today. This expulsion of gases from Earth’s interior is a process known as outgassing. The water vapor expelled by the hot, volcanic Earth in turn created clouds, which produced rain.

Over time, the rain would accumulate in basins as rivers, lakes and oceans. These basins in turn acted as sinks for accumulated carbon dioxide, which later became locked into deposits of limestone and other sedimentary rocks. Nitrogen, which is not chemically active, accumulated in the atmosphere. Any significant amounts of oxygen probably did not exist in Earth’s early atmosphere.

Only when tiny bacteria living in Earth’s oceans developed the ability to split water molecules apart by using the energy of sunlight could any significant amount of oxygen begin to accumulate in the atmosphere. It was these processes that are believed to have produced the modern atmospheric composition of 78% nitrogen and 21% oxygen.

Organization of the Atmosphere
The atmospheric layers are in order from sea level to space:

Troposphere
The troposphere is where all weather takes place. It is a region of rising and falling pockets of air moving mostly vertically.

The troposphere's height varies between seasons and latitudes, with the equator having the highest troposphere (12-16 km) and the poles the lowest (8km).

Stratosphere
The stratosphere is located above the troposphere, separated from it by the tropopause. Airplanes fly into the lower levels of the stratosphere above the clouds. Most clouds cannot form in the stratosphere because its temperature inversion inhibits convection. As a result, airflow in the stratosphere is mostly horizontal.

The stratosphere contains the ozone layer, which absorbs the majority of dangerous UV radiation from the sun. It is also the cause of the stratosphere's temperature inversion, because the ozone layer is very warm from absorbing so much radiation.

Mesosphere
Above the stratosphere is the mesosphere. In the mesosphere, temperatures drop with increasing altitude.

In the mesosphere, meteors start to disintegrate due to collisions with gas molecules.

Thermosphere
The outer-most layer. Though the thermosphere has a very high temperature since the molecules move very fast, it has a very low thermal energy because the molecules are spaced so far apart, and so a section of space in the thermosphere would contain very few molecules. (Remember that temperature is the average kinetic energy of each molecule, while thermal energy is total kinetic energy. Neither is to be confused with heat, which refers to the transfer of thermal energy from a hotter object to a cooler one.)

It is important to know how temperature changes within each layer (see right)

Some more current publications list the Exosphere as the outermost layer

Atmospheric Circulation
Let’s take a look at the motion of the atmosphere on a global scale and look at how it's associated with everyday weather.

A non-spinning planet with no axial tilt would only experience the influence of unequal heating by the Sun, with the most direct sunlight reaching the tropics and the least amount reaching the polar regions. Under these circumstances, a simple convection system would suffice with extreme heating in the low latitudes causing warm air to rise.

When this rising air mass reaches the top of the tropopause it stops its upward movement and begins to move towards the poles as an upper level wind.

Cooling air at the Polar Regions encourages the air to sink downward and fall towards the surface. At the surface, this cold air then begins to flow towards the equator.

These convection cells transfer heat by the movement air from the equator towards the poles and then cycle air near from the surface to the equator forming the basis of the two cell model.



Air Pressure
Atmospheric pressure is the weight of the overlying column of air. As altitude increases, the amount of overlying air in the atmosphere decreases, and so air pressure decreases, and vice versa.

Around 80% of the mass of Earth’s atmosphere is within the closest 18km to its surface. This is because the air itself is affected by air pressure; the higher air pressures closer to sea level cause the air to be more compressed than at high elevations.

Atmospheric pressure is normally measured in units called millibars (mb). One millibar is equal to 1 gram per centimeter squared (1g/cm2).

At sea level, the average air pressure is 1,013mb. At the top of Mt. Everest the air pressure can get as low as 300mb. Although the concentration remains the same, the amount of oxygen in the atmosphere is decreased at higher elevations because of the lower air pressure, as the pressure of gases such as oxygen is related to density. That means there is only about 1/3 as much oxygen on Mt. Everest as there is at sea level. This why many people who attempt to climb Mt. Everest experience shortness of breath as they climb to higher elevations.

Descending air forms high pressure centers, or divergence.

Polar highs result from the descent of cold air and its movement towards onto the surface. Subtropical highs form as warm air in the 20-30° latitude range in both hemispheres rises and then begins to cool as it falls towards the surface. This air is very dry making surface conditions in these regions very arid. Most of the world’s deserts in both hemispheres are found in this latitude range. High pressure cells move in a clockwise direction in the Northern Hemisphere.

Ascending air forms low-pressure systems or areas of convergence. Tropical lows form as warm air ascends up into the atmosphere. Sub polar lows form as warm air in the 50-60° latitude ranges of both hemispheres rises producing abundant precipitation. Low-pressure cells move in a counterclockwise direction in the Northern Hemisphere.

Air tends to move from areas of high to low pressure. Air is denser in high-pressure cells (anticyclones), which tend to be hot and dry: this is because air tends to heat up when compressed (adiabatic warming), evaporating clouds and leading to drier weather. The evaporation of clouds also decreases surface albedo (reflectivity).

Low-pressure cells tend to bring precipitation because they draw air upwards, and the reduced pressure and temperature at higher altitudes cause water vapor to condense into clouds. Low-pressure areas (or cyclones) are often formed by warm, moist air evaporating over oceans.

Coriolis Effect and the Three Cell Model
If the Earth did not rotate on its axis, there would be a single circulation cell in each hemisphere. The rotation of the earth on its axis from west to east creates the Coriolis Effect, which causes the different air masses created by the unequal heating of the planet’s surface to shift directionlike the picture on the left (click on it to get a better view). Notice the deflection created by the Coriolis Effect and how it changes in each hemisphere and in different regions of each hemisphere.



The Coriolis Effect causes wind patterns in the Northern Hemisphere to differ from wind patterns in the Southern Hemisphere. In the Northern Hemisphere, the Coriolis Effect deflects the movement of air to the right. In the Southern Hemisphere, this movement is deflected to the left. This creates the three main wind belts found at the surface of each hemisphere including the easterly trade winds, prevailing westerlies and the polar easterlies.

Three Cell Model
The Coriolis Effect turns the high and low pressure cells of each hemisphere into a series of three different convection cells known as the Hadley Cell, the Ferrel Cell and the Polar Cell. All three are found in both hemispheres.



The three cell model shows the Earth's global winds and the global circulation of air in the form of convection cells, which are separated by pressure belts.

The polar high is found at the poles, which are also the center of the polar cells, and therefore the Polar Easterlies.

The Polar Cell which is the cold high pressure cell around the poles. The winds in this cell blow like as expected with the Coriolis Effect, creating the Polar Easterlies

In between the Polar Cell and the next cell (Ferrel Cell) there is a subpolar low.

Next is the Ferrel Cell, which is the mid latitude cell and is a warm cell. The Ferrel Cell also contains the Prevailing Westerlies.

In between the Ferrel Cell and next cell (Hadley) there is a subtropical high.

The Hadley cell is also a warm cell and the winds again blow as expected with the Coriolis Effect, creating the Northeast Trade Winds in the Northern Hemisphere and the Southeast Trade Winds in the Southern Hemisphere.

The Real World
The real world screws up the concept of the Coriolis Effect

Take this picture for example

As shown, the winds are blowing in the "wrong" direction according to the Coriolis effect, right?

It is noted above that the global cells and the Prevailing Westerlies seem to be blowing "backwards" in is the Ferrel Cell.

This happens because winds blow from high pressure to low pressure. There is a subtropical high at 30 degrees and a sub polar low at 60 degrees, therefore the wind blows from 30 degrees to 60 degrees. That wind is still subject to the Coriolis Effect, therefore it still curves, it is just affected differently.

Planetary Winds
Global scale winds are winds that are created in the different Global circulation Cells.
 * 1) Polar Easterlies
 * 2) Prevailing Westerlies
 * 3) Trade Winds

The Polar Easterlies blow from the poles to 60˚ latitude.

The Prevailing Westerlies blow from 60˚ to 30˚ latitude.

The Trade Winds blow from 30˚ latitude to the equator.

Mountain/Valley Winds
During the day, mountains warm, causing the air over them to be warmer than the air over the valley at the same elevation. Warming the air causes it to rise up, creating a valley wind. During the evening, the air cools due to a loss of surface energy to space. The cool dense air moves down slope as a mountain wind.

Chinook Winds
A Chinook wind is a warm dry wind on the leeward side of a mountain. As air descends the leeward side of a mountain (also known as the "Rain Shadow"), it is compressed and adiabatically heated. Warming the air causes the saturation point to increase, causing a decrease in its relative humidity. The new warm and dry wind moves down slope rapidly, and during the spring causes substantial melting of mountain snow. A Chinook is a FOEHN wind that is specific to the Rocky Mountains.

Santa Ana Winds
Santa Ana winds are warm and dry winds. Over plateau regions in the desert region of the United States, high pressure pushes the air off the plateaus, forcing the air into narrow mountain valleys. As the air is forced through the valley it compresses and warms. As the air warms the saturation point rises and its relative humidity drops.

Earth Energy Budget
The Earth’s Energy Budget is determined by the amount of incoming energy and the amount of outgoing energy. Nearly all of Earth’s incoming energy (99.98%) is from solar radiation. About .013% comes from geothermal energy that is created by the radioactive decay of Earth’s core. About .002% of Earth’s incoming energy comes from the action of tides caused by the interaction of Earth with the Sun and Moon. Waste heat energy from fossil fuel consumption accounts for about .007% of Earth’s Energy Budget. The Earth has an average albedo of about 30% which means that ~30% of incoming solar radiation is radiated back into space before it reaches Earth's surface. After the 30% the atmosphere absorbs 19% and the earths surface absorbs 51%.

Around 70% of solar energy that is absorbed by the Earth is reradiated as infrared energy. The Earth’s Energy Budget is in equilibrium as the amount of incoming energy is balanced by the same amount of outgoing energy.

Convection
Convection is the transfer of heat from the Earth’s surface into the atmosphere. When a layer of air receives enough heat, it expands and is pushed upward by buoyancy. Then air becomes denser and moves laterally until it begins to sink and then begins to rise again as it warms. Atmospheric convection currents may cause breezes, winds, cyclones and thunderstorms.



Radiation Budget
Radiation budget refers to the balance between incoming radiation from the Sun and the outgoing thermal, or longwave and reflected shortwave energy from Earth. Globally the budget is balanced as the amount of incoming solar radiation is transformed into latent heat, or even kinetic energy. Energy transfers in the oceans along with the atmosphere keep the radiation budget in balance.

But locally the Radiation Budget is unbalanced because tropical regions retain more insolation, while less is retained in higher latitudes.This accounts for differences in the temperature and pressure of air masses that originate in both regions affecting weather throughout the planet

Air Masses
Large bodies of air that pass slowly over large areas of Earth’s surface and they take on the characteristics of that region such as temperature and humidity. The area from which the air mass derives its characteristics is its source region.

Air mass source regions can be snow covered areas near the poles,arid deserts, or even tropical oceans.

Air masses that form over the ocean are termed maritime air masses.

Those that form over land are called continental air masses.

Any further classification of air masses are normally based on longitude. Tropical air masses are formed in low latitudes. Polar are formed in high latitudes.

Classifications


The major air masses that influence the United States are:

Polar air masses that form over Canada and Alaska often affect the weather of the United States as they move south and eastward.

The states along the Gulf of Mexico and the Eastern seaboard often experience the effects of tropical air masses that move northward cuasing humid subtropical and continental climates.

Occasionally, continental arctic (cA) air masses may descend from high latitude regions in the winter months creating bitterly cold weather.

Tropical air masses from the Pacific may affect California and the Southwestern states during the winter months. Although it is influenced by these major air masses, the United States itself is not a favorable source region for fronts because so many weather disturbances disrupt opportunities for the formation of air masses.

Air masses move from their source region due to the Coriolis Effect where they will meet adjacent air masses with different properties. When these two air masses of different origin meet, the boundary between them is termed a front.

Fronts
Frontal boundaries are very narrow, less than 200km wide. Normally one air mass is cooler than the other, giving the warmer air a tendency to flow up and over the cooler air mass. This cooler and denser air acts as a wedge that allows warmer less dense air to rise over it.

Types
There are five types of fronts, each with their own characteristics.
 * 1) Warm Front
 * 2) Cold Front                     [[image:cold.jpg|thumb|200px|Cold Front]]
 * 3) Stationary Front            [[image:warmfront.jpg|thumb|200px|Warm Front]]
 * 4) Occluded Front
 * 5) Dry Line

Warm Fronts
A warm front is when warm air moves in and displaces an area of once cooler air. Warm fronts are characterized by an increase in temperature and the appearance of cirrus clouds.
 * shown on a map as semicircles
 * clouds become lower as front nears
 * Slow rate of advance
 * light to moderate precipitation
 * gradual temperature increase

Cold Fronts
Cold fronts are formed when cooler air replaces an area that was once occupied by warmer air. They are associated with turbulent changes in weather. Temperatures drop as warm air is pushed aside vertically and abruptly. Tall, cumulonimbus clouds take shape and may form thunderstorms.
 * shown on a map as triangles
 * cold air replaces warm air
 * weather is more violent than warm front
 * faster rate of advance
 * precipitation intense
 * clear after front passes

Stationary Fronts
Nearby stationary fronts bring weather patterns that may persist for days.
 * shown on a map as alternating triangles and semicircles facing in opposite directions
 * air flow parallel on both sides
 * doesn't move
 * widespread clouds
 * Precipitation light

Occluded Fronts
Occluded fronts occur when a cold front overtakes a warm front. This often results from the merging of two cold fronts that overwhelm the warm front. The result is a weakening of the storm system that might otherwise occur.


 * active cold front overtakes a warm front
 * weather is complex
 * precipitation associated with warm air

There are two types of occluded fronts, known as cold occlusion and warm occlusion. In cold occlusion, the approaching cold air mass creating the cold front is colder than the retreating cold/cool air mass in front of the warm front. The opposite is true for warm occlusions, where the cold/cool air mass creating the cold front is warmer than the retreating cold air mass in front of the warm air mass. Also to note, cold occlusions are much more common than warm occlusions.

Dry Lines
A dry line is a line that separates a moist air mass from a dry air mass. It can also be referred to as a dew point front because the dew point temperature changes drastically across the dry line. The most common place to find a dry line is just east of the Rocky mountains separating the dry air that comes over the mountains from the moist air coming off of the Gulf of Mexico and the Atlantic ocean. Dry lines are extremely rare east of the Mississippi River.

Water in the Atmosphere
The atmosphere of our planet is laden with water. In temperate and tropical regions, water exists mainly in liquid form. At the poles and higher latitudes, much of Earth’s water exists as ice locked away in alpine or continental glaciers. The physical composition of Earth’s atmosphere consists primarily of water vapor.

Humidity refers to the amount of water vapor that is in the air. This water vapor exists in a gaseous state. The process in which water changes from a liquid into a gaseous state is evaporation. Each water molecule that becomes water vapor also takes with it a parcel of heat energy from the surface it evaporates from cooling the surface (evaporative cooling). Evaporative cooling explains why someone may feel a chill after swimming as water evaporates off the surface of their skin, taking with it heat from their body.

During the spring when the amount of daylight is increasing and the declination of the hemisphere is tilting towards the Sun, the intensity of solar radiation increases causing ice crystals in the upper troposphere to melt and fall as rain. As the water is exposed to increased solar radiation it evaporates and returns to the atmosphere in a gaseous state-as water vapor. The humidity of the atmosphere increases as spring changes to summer.

Water vapor is measured using an instrument known as a hygrometer. Measurements of humidity are often expressed as a percentage, which is termed relative humidity. The complete saturation of the air (100% relative humidity) occurs when the amount of water vapor in the air equals the amount of water vapor that the air can hold.

Precipitation
Precipitation is any form of water that falls to the surface of Earth. The most common forms precipitation occurs in are:
 * rain
 * snow
 * sleet
 * hail

Liquid Precipitation
Mist consists of droplets less than .05mm in diameter. Drizzle is anything larger than.05mm but less than .5mm larger than 0.5mm across is rain. Most raindrops are not larger than 5mm across because of air drag effects that would tear larger droplets into smaller droplets as they descended through the air.

Frozen Precipitation
Snowflakes fall as ice crystals and have diameters of between 1mm and 2cm. They form through deposition of water vapor onto particles such as dust, and the water vapor is directly converted into ice.

Graupel is around 5mm and falls as soft and mushy ice.

Sleet is similar to graupel, but it is smaller, forming when raindrops freeze as they fall.

Hail is larger than 5mm and is formed from rounded clumps of hard, layered ice. It is usually associated with thunderstorms. Each individual hailstone is repeatedly cycled through the interior of a thunderstorm by strong updrafts, allowing layers of ice to accumulate before it finally becomes too massive and falls to the ground.

Another variation is rime, a deposit of ice that freezes onto a surface that has a temperature below 0°C. Rime forms from water droplets that are supercooled: below the freezing point, but unable to freeze into ice until coming into contact with something (similar to the concept of supersaturation). Rime droplets are very small, and can often be observed on snowflakes.

Graupel essentially consists of snowflakes that have accumulated large masses of rime, to the extent that the original snowflake's structure is completely obscured.

Virga
Virga-precipitation that falls from clouds but evaporates while falling and never reaches the surface of the Earth.

At high altitudes, precipitation falls mainly as ice crystals before they melt and evaporate before reaching the ground because of compressional heating that occurs as a result of increasing air pressure closer to the ground (remember- air that is compressed becomes warmer).

Streams of falling precipitation that never reach the ground make the clouds appear to have commas attached to them as aloft winds push the bottom ends of the virga into angles. Virgas can be hazardous to pilots because the pockets of extremely cold air descending from the upper atmosphere can create microbursts.

Formation of Clouds
Clouds are nothing more than small droplets of water and ice crystals that clump together within the atmosphere. They may produce precipitation in the form of liquid water and/or ice crystals that fall to the Earth’s surface. Rising air is an important process in the formation of clouds. As air rises, it expands causing it to lose heat energy and voila the temperature of the air decreases. The water vapor molecules that are in the air also increase the humidity of the air until it is saturated (100% relative humidity).

Excess water vapor condenses changing from a gas into a liquid on large aerosol particles in the atmosphere if the relative humidity is not in excess of 100%. When the atmosphere cools, it will reach the point at which the air is saturated with water vapor and can precipitate.This is the dew point. The dew point is defined as the temperature to which a particle of air would need to be cooled in order to reach this point of saturation. The air’s capacity to hold water vapor is temperature dependent. Warmer air tends to hold more moisture, while cooler air holds less.

The dew point and relative humidity can be measured using a psychrometer, a weather measurement tool consisting of two identical thermometers mounted side by side. One of the thermometers- the dry bulb measures air temperature. The other thermometer- the wet bulb- has a damp wick wrapped around it allowing it to measure any decrease in temperature. This indicates the maximum amount of cooling that can result from evaporation.

To use a psychrometer, it needs to be exposed to a flow of air by slinging it around on a handle. The humidity of the air is directly proportional to the amount of moisture evaporating off the wet bulb. If the two thermometers have identical readings, than no evaporation has taken place and the air is saturated with water vapor. The more significant the measured difference between the two thermometers, the drier the air and the lower the level of humidity.

Cloud formation is closely related to the cooling of humid air masses. As water vapor expands- it cools in temperature. Likewise, when air is compressed- it heats up. This change in temperature caused by the expansion or contraction of gases is known as adiabatic temperature change. This is a cooling or warming of the air caused by expansion or contraction and not by the increase or irradiation of heat.

The effects of adiabatic temperature change in Earth’s atmosphere can be dramatic. Air sinking down from higher latitudes is warmed by an increase in atmospheric pressure as it contracts. Likewise, warm air that climbs in altitude is under less pressure and cools as it expands. When this air is enriched in water vapor and cooled down to its dew point, condensation and cloud formation can take place.

Cloud ID
It is imperative to be able to identify clouds and the weather associated with each cloud. Cloud prefixes tell where the clouds are located.

"cirr-", like cirrus clouds, can be located at high levels

"alto-", like altostratus, can be found at middle levels

Cloud types are classifies by height of the ground these are three of the classifications This is a list identifying which clouds go in which layer. These are from "The cloud book: how to understand the skies" by Richard Hamblyn
 * Upper Clouds
 * 9000 meters
 * Cirus clouds
 * Intermediate Clouds
 * 3000-7000 meters
 * Altocumulus
 * Lower Clouds
 * 2000 meters
 * Nimbostratus
 * High Fogs
 * Under 1000 meters
 * 1) Low Clouds
 * 2) Stratocumulus
 * 3) Stratus
 * 4) Cumulus
 * 5) Medium Clouds
 * 6) Altocumulus
 * 7) Altostratus
 * 8) Nimbostratus
 * 9) High clouds
 * 10) Cirrus
 * 11) Cirrocumulus
 * 12) Cirrostratus
 * 13) Multi-level
 * 14) Cumulonimbus

Clouds
Great Cloud page http://ww2010.atmos.uiuc.edu/(Gh)/guides/mtr/cld/cldtyp/home.rxml

Great Cloud book is "The cloud book: how to understand the skies" by Richard Hamblyn



Optical Phenomena
There are many types of weather phenomena but here are the major ones.

Forecasting
There are many ways to forecast, but the simplest way is to take today's weather and say that tomorrow is going to be the same. This can be called the Persistence method. This method is useful in some places (e.g., Florida during the summer) but can also be very unreliable in other places (e.g., Chicago during the spring).

The next method can be called the trends method it relies on mathematics to forecast. This method involves being able to get a accurate measurement of the speed at which the weather system is moving and putting the numbers into(S=d/t) and determining the time at which the system will be at a position. Here is an example of the trend model:

The Climatology Method is another easy way of forecasting. This method involves averaging weather statistics accumulated over many years to make a forecast.

The Analog Method is a more complicated method of producing a forecast. It involves examining today's forecast scenario and remembering a day in the past when the weather scenario looked very similar. The Analog Method uses that previous information to predict that today's weather will be similar.

Radar
Before we get into any satellite imagery or the like, it is important to understand Radar. Radar is a very important part of today's meteorology. It gives us a chance to have early warning of approaching storms and rain. So lets start with the basics.

Radar Basics
Radar is a simple concept, a beam is sent out and reflects back to an antennae that collects the beam and sends it via wire to a receiver. The return signals are arranged to produce a radar image.



So when the beam of energy (electromagnetic) hits it target it is reflected in all directions, some going up, some going down, some going back toward its origin point. The most important part is the returning energy. This returning energy is much weaker when it is returning than when it left. The size of the reflecting particle determines the strength of the return signal. This means that the larger the particle, the stronger the signal, and the smaller the particle, the weaker the signal. Also the more particles there are, the stronger the return signal because the returning beams combine to form a stronger signal

The amount/size of the reflectivity is proportional to the number and size of the drops encountered by the electromagnetic pulse. Because of this high reflectivity normally means heavy precipitation while low reflectivity means lighter precipitation.

Since radar uses electromagnetic pulses or electromagnetic waves, wavelength will affect the signal and pulses. The two wavelengths are short and long wavelengths. Short wavelengths are good at measuring small particles like dust and cloud droplets. However the short wavelengths are also easily absorbed by the the materials it reflects off of (this is called attenuation). This feature makes it hard to measure distant targets.

Long wavelengths have the advantage that absorption by the particles is reduced. This feature makes this wavelength very useful for looking at severe storms and other large scale/distant weather. Long wave radar is used in most Doppler radars like the National Weather Service's WSR-88D (NEXRAD) Doppler radars.

How To read weather maps/satellite imagery


A good place to start is a basic weather map, the kind that is frequently seen at competitions:
 * 1) Start by identifying the different pressure zones on the map. Above it is already done but if it wasn't marked look for sections that have a circle with a very high or low pressure.
 * 2) Look for fronts. This can be done by looking at the station ball symbols. (those are the yellow circles with the tails the tails indicate wind direction) look and find a sudden change in wind direction/pressure that will normally indicate a front. I marked where I believe a front to be.

There are many lines on this map. Each one means something:
 * The blue lines are isobars which mean that they are lines of constant pressure.
 * The yellow circles with "tails" are called station ball symbols of station models; they are explained in the next section.

Another feature that is common on weather maps are isotherms. Isotherms ("Iso" coming from the Greek word "Isos" meaning "equal", and "Therm" coming from the Greek word "Thérmē" meaning "heat") are lines drawn across the map that connect points that have the same temperature.

Station Models


This image is a station model. It can tell many different measurements, such wind speed, wind direction, temperature, dew point, current weather, cloud cover, and pressure. Some symbols have more information than others on them, but here is a basic overview:


 * The 48 is the current temperature
 * The 45 is the dew point
 * The "whatever" that is in between the two numbers is the current weather. On this one it is a light rain.



This is what tells information about the wind. The direction the stick faces shows the wind direction, and how many lines on the end of it show the wind speed. A half line signifies five knots, a full line ten knots, and a bold line 50 knots.



This indicates how much cloud cover there is. There are nine choices:

Symbols
this is from here:http://www.sover.net/~redcamp/wxplegend.gif

another symbol sheet with two examples

Rawinsondes/Radiosondes
Rawinsondes and Radiosondes are interconnected they both are part of the weather equiptment luanched in weather balloons.

A radiosonde or rawinsonde will normally record and "observe"
 * Pressure
 * Altitude
 * Location (coordinates)
 * Temperature
 * Wind speed and direction

METAR
This is a way that meteorologists convey what is happening at a point on Earth. It is a very abbreviated language. Here is an example of METAR:

KCLL 312253Z 14007G15KT 10SM CLR 31/15 A2990 RMK AO2 SLP120 T03110150

Zulu is a time measurement based off of a 24-hour clock

here is a more in depth METAR guide: http://www.met.tamu.edu/class/metar/quick-metar.html

Stuve Diagrams
A Stuve diagram is the compilation of data gathered in Weather Balloon flights.



As seen, the image above is extremely cluttered and hard to understand so lets break it down.



This image shows the Stuve diagram at is most basic level. The left Y-axis shows air pressure and elevation (in meters).

The X-axis shows temperature in Kelvin and well as Celsius.

Now that we have the X and Y axes in order, lets talk about the yellow horizontal and vertical lines that look similar to graph paper except are not constant. The vertical lines represent isotherms, or lines of constant temperature and the horizontal lines represent isobars, or lines of constant pressure. Since the axis and lines are down, direct your view to the "barbs" along the right side, which show wind speed and direction. They are on the same scale as the Station Model symbols.

Now that everything is clear, lets get to what I bet you have been staring at since you first started; The red line. The red line shows the relationship between air temperature and altitude.



As you can see more information has been added; the dashed green lines and the dashed black line.

The dashed green line shows represents the saturation mixing ratio which is the amount of water vapor needed in a parcel of air (the amount needed to make a cloud).

The black line shows how the dew point temperature changes with altitude.



Since it makes it more interesting, lets add yet more elements to this chart. These are the yellow line and also the solid diagonal lines.

The yellow line show the temperature of a parcel of air as it is moved through the atmosphere. The solid diagonal lines are called dry adiabats and show the rate at which unsaturated of dry air will cool down as it rises up through the atmosphere, at a rate of about  10˚C/km.

If an air parcel is initially unsaturated, it will cool off at the dry adiabatic lapse rate as it rises (note that the yellow line is parallel to the solid diagonal lines).

So let us assume the parcel of air starts off at an altitude of 500m with a temperature of 22˚C. If it gets lifted up, it will cool off at 10ºC for every km it rises. This is shown by the yellow line. At an altitude of 2000m it will have cooled to a temperature of about 7˚C. At this point it has cooled down enough that it is now saturated.

Why does this happen? Remember that the saturation mixing ratio for any temperature and pressure can be found using the dashed green lines on the graph.Well, at 800 mb and 7˚C (where the yellow line ends) the dashed green line which would go through this point would have a value of 8 g/kg. This is the saturation mixing ratio for this point. But this was also the actual mixing ratio for this air parcel. So now the air has cooled down enough that the actual mixing ratio is the same as the saturation mixing ratio. The altitude at which this happens is the lifting condensation level (LCL). This is the point at which moisture contained in a rising parcel of air can begin to condense. this is shown in the list of data at the right-hand side of the figure. Look under “PARCEL”, then find “LCL:800”. This indicates that the lifted air parcel would reach its lifting condensation level at 800 mb.



Finally, the last part of a Stuve diagram are the solid green lines which are referred to as saturated adiabats. These show the rate at which saturated air cools as it rises.

The lines are somewhat curved because the saturated adiabatic lapse rate fluctuates between 2˚C/km to nearly 10˚/km (the dry adiabatic lapse rate), depending moisture content of the parcel of air

Images above come from this site

Meteograms
A meteogram is a mix of station ball symbols and metar

The graph along the top of the Meteogram shows temperature and Dew point. temperature is the top line(green) and dew point is the bottom line (blue)

The abreviation EXTT (extreme temperature) shows the maximum and minimum temperatures which are plotted below the chart at specific reporting times. 12Z and 18Z are generally low temperatures and 0Z and 6Z are high temperatures.

The WX shows the current weather data at the time of data collection

SNWDP shows snow-depth if there is any.

PREC tells precipitation in inches

VIS tells visibility in miles

WGST tells wind gusts

WIND (winds and cloud cover) - This is same sympols wind and cloud cover symbols used in the station models

Cloud chart will give cloud layer information. The vertical axis is height of cloud base in feet. The layers are plotted as horizontal lines.
 * Clear skies are plotted as a 'C'.
 * Scattered cloud layers (1/8th to 3/8th coverage) are plotted as a single short dash.
 * Broken cloud layers (4/8th to 7/8th coverage) are plotted as two short dashes. *Overcast layers are plotted as a single long dash.

The actual cloud ceiling is displayed below the chart in 100s of feet if the ceiling is below 10,000 feet.

Pressure chart - This chart plots sea level pressure (or altimeter setting if pressure not reported) in millibars.

Terms To Know
Some basic terms

Here is an explanation of degree days.

From a meteorological standpoint, degree days are defined with respect to 65 F as a reference point. The National Weather Service calculates it as follows: Heating Days / Cooling Days The daily high and low temperature, both measured to the nearest whole degree Fahrenheit, are averaged. If the average is not an integer, it is rounded up. Subtract this average from 65. If it is a positive quantity, it is the number of COOLING degree days for that day. If it is negative, its absolute value is the number of HEATING degree days.

As an example, yesterday in Omaha, Nebraska the high was 55 and the low 28. Averaging those two numbers:

Average = (High + Low)/2 = (55 + 28)/2 = 83/2 = 41.5. This needs to be rounded up to 42 (it is always rounded up).

Degree Days = Average - 65 = 42 - 65 = -23. It's negative so yesterday there were 23 HEATING degree days in Omaha.

Degree days are reported daily in climate summaries issued by the National Weather Service. Monthly and yearly sums of the daily degree days are also reported. Counts for heating and cooling degree days are kept separate.

Note: the "year" for heating degree days is typically that sum from the period July 1-June 30, while cooling runs from January 1-December 31.

Degree days can be calculated with other reference values than 65, but the National Weather Service standard is 65 degrees.

Links
This is a great meteorology site and some of the images on this page have come from here

Also, see these Everyday Weather Meteorology Notes

EpicFailOlympian's Everyday Weather Notes