a http-equiv="Content-Type" content="text/html; charset=iso-8859-1">Prevailing Winds

Flight Environment

PREVAILING WINDS

HEMISPHERICPREVAILING WINDS

Due to the fact that the atmosphere is addressed to the earthby gravity and also rotates with the earth, tright here would certainly be no circulation if some force did notupcollection the atmosphere"s equilibrium. The heating of the earth"s surconfront by the sunlight isthe pressure responsible for creating the circulation that does exist.

You are watching: A steep pressure gradient ________.

Since of the curvature of the earth,the the majority of direct rays of the sun strike the earth in the vicinity of the equator resultingin the best concentration of heat, the largest possible amount of radiation, and themaximum heating of the setting in this area of the earth. At the exact same time, thesun"s rays strike the earth at the poles at a really oblique angle, causing a muchlower concentration of heat and also much much less radiation so that tright here is, in reality, exceptionally littleheating of the atmosphere over the poles and also in turn extremely cold temperatures.

Cold air, being even more dense, sinks andwarm air, being much less thick, rises. Consequently, the climbing warmth air at the equatorbecomes also much less thick as it rises and also its pressure decreases. An location of lowpress, therefore, exists over the equator.

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Warm air rises till it reaches aspecific elevation at which it starts to spill over right into bordering areas. At thepoles, the cold thick air sinks. Air from the top levels of the atmosphere flowsin on optimal of it boosting the weight and creating an area of high press at the poles.

The air that rises at the equator does notflow directly to the poles. Due to the rotation of the earth, there is a build up of airat about 30° north latitude. (The exact same phenomenon occurs in the Southern Hemisphere). Several of the air sinks, bring about a belt of high-pressure at this latitude.

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The sinking air reaches the surfaceand flows north and also south. The air that flows southern completes one cell of theearth"s circulation pattern. The air that flows north becomes component of one more cellof circulation in between 30° and 60° north latitude. At the same time, the sinkingair at the north pole flows southern and collides with the air relocating north from the 30°high pressure location. The colliding air is required upward and also an area of low pressureis developed close to 60° north. The third cell circulation pattern is produced betweenthe north pole and also 60° north.

Because of the rotation of the earthand the coriolis pressure, air is deflected to the ideal in the Northern Hemisphere. Asan outcome, the motion of air in the polar cell circulation produces the polar easterlies. In the circulation cell that exists between 60° and also 30° north, the movement ofair produces the prevailing westerlies. In the tropic circulation cell, thenortheast profession winds are produced. These are the so-dubbed permanent wind systemsof the each.

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Because the earth rotates, the axis is tilted, and tright here is more land mass in the northern hemispbelow than in the southern hemisphere, the actual worldwide pattern is much even more complicated. Instead of one large circulation in between the poles and the equator, tright here are 3 circulations...Hadley cell
- Low latitude air activity towards the equator that with heating, rises vertically, via poleward activity in the upper setting. This creates a convection cell that dominates tropical and sub-tropical climates.Ferrel cell - A mid-latitude mean atmospheric circulation cell for derekwadsworth.com named by Ferrel in the 19th century. In this cell the air flows poleward and also eastward near the surface and equatorward and also westward at higher levels.Polar cell - Air rises, diverges, and also travels toward the poles. Once over the poles, the air sinks, developing the polar highs. At the surconfront air diverges external from the polar highs. Surchallenge winds in the polar cell are easterly (polar easterlies).

UPPER LEVEL WINDS

Tbelow are 2 main forces which influence the movement of air in the top levels. The press gradient reasons the air to move horizontally, forcing the air directly from a region of high pressure to a region of low pressure. The Coriolis force, but, deflects the direction of the flow of the air (to the best in the Northern Hemisphere) and causes the air to circulation parallel to the isobars.

Winds in the top levels will blow clockwise about locations of high push and counterclockwise roughly areas of low press.

The rate of the wind is figured out by the pressure gradient. The winds are strongest in regions where the isobars are close together.

SURFACE WINDS

Surface friction plays a crucial role in the speed and direction of surconfront winds. As a result of the slowing dvery own of the air as it moves over the ground, wind speeds are much less than would be intended from the push gradient on the derekwadsworth.com map and also the direction is readjusted so that the wind blows throughout the isobars into a center of low pressure and out of a facility of high push.

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The effect of friction normally does not extfinish more than a pair of thousand also feet right into the air. At 3000 feet above the ground, the wind blows parallel to the isobars with a rate proportional to the push gradient.

Even enabling for the results of surface friction, the winds, locally, perform not constantly show the speed and direction that would be supposed from the isobars on the surface derekwadsworth.com map. These variations are generally due to geographical attributes such as hills, hills and also huge bodies of water. Except in mountainous areas, the impact of terrain attributes that cause regional variations in wind extends typically no greater than about 2000 feet above the ground.

LAND AND SEA BREEZES

Land and also sea breezes are resulted in by the distinctions in temperature over land and also water. The sea breeze occurs in the time of the day as soon as the land also location heats more quickly than the water surchallenge. This results in the press over the land also being lower than that over the water. The push gradient is often strong enough for a wind to blow from the water to the land.

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The land also breeze blows at night as soon as the land also becomes cooler. Then the wind blows towards the warmth, low-push area over the water.

Land and also sea breezes are incredibly neighborhood and also impact just a narrow area along the shore.

MOUNTAIN WINDS

Hills and valleys dramatically distort the aircirculation associated via the prevailing press mechanism and the push gradient. Strong up and down drafts and eddies develop as the air flows up over hills and down into valleys. Wind direction changes as the air flows about hills. Sometimes lines of hills and also mountain ranges will act as a barrier, holding ago the wind and also deflecting it so that it flows parallel to the array. If there is a pass in the mountain selection, the wind will certainly rush through this pass as via a tunnel via significant rate. The airflow deserve to be supposed to reprimary rough and erratic for some distance as it flows out of the hilly location and also right into the flast countryside.

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Daytime heating and also nighttime cooling of the hilly slopes bring about day to night variations in the aircirculation. At night, the sides of the hills cool by radiation. The air in contact with them becomes cooler and also therefore denser and it blows dvery own the slope into the valley. This is a katabatic wind (sometimes likewise called a hill breeze). If the slopes are spanned with ice and also snow, the katabatic wind will certainly blow, not just at night, but likewise throughout the day, carrying the cold dense air right into the warmer valleys. The slopes of hills not extended by snow will be wequipped throughout the day. The air in call via them becomes warmer and also much less dense and, therefore, flows up the slope. This is an anabatic wind (or valley breeze).

In mountainous areas, regional distortion of the aircirculation is even more significant. Rocky surencounters, high ridges, sheer cliffs, steep valleys, all integrate to create unpredictable circulation trends and also disturbance.

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THE MOUNTAIN WAVE

Air flowing across a hill array commonly rises fairly smoothly up the slope of the range, however, once over the optimal, it pours down the other side through significant force, bouncing up and also dvery own, creating eddies and also disturbance and also creating powerful vertical waves that might extfinish for excellent ranges downwind of the hill variety. This phenomenon is known as a mountain wave. Note the up and dvery own drafts and also the rotating eddies developed downstream.

If the air mass has actually a high moisture content, clouds of incredibly distinctive appearance will build.

Cap Cloud. Orographic lift reasons a cloud to develop alengthy the optimal of the ridge. The wind carries this cloud down along the leeward slope wright here it dissipates through adiabatic heating. The base of this cloud lies close to or below the peaks of the ridge; the top might reach a few thousand also feet over the peaks.

Lenticular (Lens Shaped) Clouds develop in the wave crests aloft and also lie in bands that might extfinish to well above 40,000 feet.

Rotor Clouds develop in the rolling eddies downstream. They resemble a lengthy line of stratocumulus clouds, the bases of which lie below the hill peaks and the tops of which might reach to a significant elevation over the peaks. Occasionally these clouds develop into thunderstorms.

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The clouds, being exceptionally distinctive, have the right to be viewed from a good distance and administer a visible warning of the hill wave condition. Unfortunately, occasionally they are installed in other cloud devices and are surprise from sight. Sometimes the air mass is very dry and the clouds execute not construct.

The severity of the hill wave and the height to which the disturbance of the air is affected is dependent on the toughness of the wind, its angle to the range and the stability or instcapability of the air. The many significant hill wave problems are produced in strong airflows that are blowing at ideal angles to the variety and also in stable air. A jet stream blowing practically perpendicular to the mountain variety rises the severity of the wave condition.

The hill wave phenomenon is not restricted only to high hill ranges, such as the Rockies, but is additionally present to a lesser degree in smaller mountain systems and also even in lines of small hills.

Mountain waves current troubles to pilots for numerous reasons:

Vertical Currents. Downdrafts of 2000 feet per minute are prevalent and downdrafts as good as 5000 feet per minute have actually been reported. They happen alengthy the downward slope and also are most serious at a height equal to that of the summit. An airplane, captured in a downdraft, can be compelled to the ground.

Turbulence is generally incredibly severe in the air layer between the ground and also the tops of the rotor clouds.

Wind Shear. The wind speed varies considerably between the crests and troughs of the waves. It is typically many major in the wave nearest the hill selection.

Altimeter Error. The rise in wind speed outcomes in an accompanying decrease in push, which subsequently affects the accuracy of the pressure altimeter.

Icing. The freezing level varies considerably from crest to tunstable. Severe icing can occur because of the big supercooled droplets sustained in the solid vertical currental fees.

When flying over a hill ridge where wave problems exist: (1) Avoid ragged and ircontinuous shaped clouds—the irconsistent shape shows turbulence. (2) Approach the hill at a 45-level angle. It you must suddenly decide to rotate earlier, a quick revolve have the right to be made ameans from the high ground. (3) Avoid flying in cloud on the mountain crest (cap cloud) bereason of strong downdrafts and disturbance. (4) Allow sufficient elevation to clear the highest ridges via altitude to spare to stop the downdrafts and also eddies on the downwind slopes. (5) Always remember that your altimeter deserve to read over 3000 ft. in error on the high side in hill wave problems.

GUSTINESS

A gust is a fast and ircontinuous fluctuation of varying intensity in the upward and also downward movement of air curleas. It may be connected with a quick adjust in wind direction. Gusts are brought about by mechanical disturbance that outcomes from friction between the air and also the ground and also by the unequal heating of the earth"s surface, specifically on hot summer afternoons.

SQUALLS

A squall is a sudden rise in the strength of the wind of much longer duration than a gust and might be resulted in by the passage of a fast relocating cold front or thunderstorm. Like a gust, it might be accompanied by a rapid change of wind direction.

DIURNAL VARIATIONS

Diurnal (daily) variation of wind is caused by strong surchallenge heating in the time of the day, which causes disturbance in the reduced levels. The result of this disturbance is that the direction and also speed of the wind at the greater levels (e.g., 3000 feet) often tends to be transferred to the surconfront. Due to the fact that the wind direction at the better level is parallel to the isobars and its rate is greater than the surconfront wind, this deliver causes the surconfront wind to veer and also boost in speed.

At night, there is no surconfront heating and also therefore less turbulence and also the surface wind has a tendency to resume its normal direction and rate. It backs and decreases. See VEERING AND BACKING section listed below for more info.

EDDIES—MECHANICAL TURBULENCE

Friction between the relocating air mass and also surface attributes of the earth (hills, mountains, valleys, trees, buildings, and so on.) is responsible for the swirling vortices of air typically referred to as eddies. They differ significantly in size and also intensity depending upon the size and roughness of the surconfront obstruction, the rate of the wind and the level of stcapacity of the air. They have the right to spin in either a horizontal or vertical aircraft. Unstable air and also solid winds produce even more vigorous eddies. In secure air, eddies tfinish to easily dissipate. Eddies produced in mountainous locations are especially effective.

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The bumpy or choppy up and also dvery own activity that signifies the presence of eddies renders it hard to store an plane in level flight.

DUST DEVILS

Dust devils are sensations that happen quite typically on the warm dry levels of mid-western North America. They deserve to be of sufficient force to present a risk to pimany light airplanes flying at low speeds.

They are small heat lows that form on clear warm days. Given a steep lapse price caused by cool air aloft over a warm surchallenge, little horizontal air movement, few or no clouds, and also the noonday sunlight heating level arid soil surencounters to high temperatures, the air in call with the ground becomes super-heated and very unsecure. This surface layer of air builds till somepoint triggers an upward activity. Once started, the warm air rises in a column and also draws more hot air into the base of the column. Circulation begins about this warmth low and increases in velocity until a small vigorous whirlwind is developed. Dust devils are usually of brief duration and also are so named bereason they are made visible by the dust, sand and also debris that they pick up from the ground.

Dust devils pose the biggest hazard close to the ground where they are most violent. Pilots proposing to land also on superheated runmethods in areas of the mid-west wright here this phenomenon is common must scan the airport for dust swirls or grass spirals that would show the existence of this danger.

TORNADOES

Tornadoes are violent, circular whirlpools of air connected through major thunderstorms and are, in truth, exceptionally deep, focused low-press locations. They are shaped prefer a tunnel hanging out of the cumulonimbus cloud and are dark in appearance because of the dust and debris sucked right into their whirlpools. They array in diameter from about 100 feet to one fifty percent mile and also move over the ground at speeds of 25 to 50 knots. Their path over the ground is normally only a few miles long although tornadoes have been reported to reduced disastrous swaths as long as 100 miles. The great destructiveness of tornadoes is caused by the extremely low push in their centers and the high wind speeds, which are considered to be as good as 300 knots.

WIND SPEEDS AND DIRECTION

Wind speeds for aviation objectives are expressed in knots (nautical miles per hour). In the derekwadsworth.com reports on US public radio and television, yet, wind speeds are provided in miles per hour while in Canada speeds are provided in kilometers per hour.

In a discussion of wind direction, the compass suggest from which the wind is blowing is taken into consideration to be its direction. Because of this, a north wind is one that is blowing from the north towards the southern. In aviation derekwadsworth.com reports, location and aerodrome forecasts, the wind is always reported in degrees true. In ATIS broadcasts and also in the indevelopment given by the tower for landing and take-off, the wind is reported in levels magnetic.

VEERING AND BACKING

The wind veers as soon as it changes direction clockwise. Example: The surface wind is blowing from 270°. At 2000 feet it is blowing from 280°. It has actually changed in a right-hand also, or clockwise, direction.

The wind backs as soon as it alters direction anti-clockwise. Example: The wind direction at 2000 feet is 090° and also at 3000 feet is 085°. It is transforming in a left-hand also, or anti-clockwise, direction.

In a descent from a number of thousand feet above the ground to ground level, the wind will generally be uncovered to earlier and also likewise decrease in velocity, as the effect of surchallenge friction becomes noticeable. In a climb from the surface to a number of thousand feet AGL, the wind will veer and increase.

At night, surface cooling reduces the eddy activity of the air. Surchallenge winds will ago and also decrease. Conversely, throughout the day, surface heating boosts the eddy movement of the air. Surchallenge winds will certainly veer and increase as more powerful winds aloft mix to the surconfront. See DIURNAL VARIATIONS area over for even more details.

WIND SHEAR

Wind shear is the sudden tearing or shearing result encountered alengthy the edge of a zone in which tright here is a violent readjust in wind rate or direction. It can exist in a horizontal or vertical direction and produces churning movements and subsequently disturbance. Under some problems, wind direction changes of as a lot as 180 degrees and rate transforms of as much as 80 knots have actually been measured.

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The impact on aircraft performance of encountering wind shear derives from the reality that the wind have the right to readjust much much faster than the aircraft mass have the right to be sped up or decelerated. Severe wind shears deserve to impose penalties on an airplane"s performance that are beyond its capabilities to compensate, particularly in the time of the crucial landing and also take-off phase of flight.

In Cruising Flight

In cruising flight, wind shear will most likely be encountered in the shift zone between the press gradient wind and also the distorted local winds at the lower levels. It will also be encountered once climbing or descending with a temperature inversion and when passing through a frontal surchallenge. Wind shear is additionally connected through the jet stream. Airplanes encountering wind shear might suffer a succession of updrafts and downdrafts, reductions or gains in headwind, or windshifts that disrupt the establimelted flight course. It is not typically a major problem bereason altitude and airspeed margins will certainly be enough to counteract the shear"s adverse effects. On occasion, yet, the wind shear may be significant sufficient to cause an abrupt increase in load variable, which could stall the aircraft or inflict structural damages.

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Near the Ground

Wind shear, encountered close to the ground, is more severe and also potentially extremely dangerous. Tright here are 4 common sources of low level wind shear: thunderstorms, frontal task, temperature inversions and solid surchallenge winds passing around natural or manmade obstacles.

Frontal Wind Shear. Wind shear is commonly a trouble only in fronts with steep wind gradients. If the temperature difference throughout the front at the surface is 5°C or more and also if the front is relocating at a speed of about 30 knots or even more, wind shear is likely to be existing. Frontal wind shear is a phenomenon connected with quick moving cold fronts but can be current in heat fronts as well.

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Thunderstorms. Wind shear, associated with thunderstorms, occurs as the result of two sensations, the gust front and downbursts. As the thunderstorm matures, solid downdrafts develop, strike the ground and also spreview out horizontally alengthy the surface well in advancement of the thunderstorm itself. This is the gust front. Winds have the right to readjust direction by as much as 180° and reach speeds as good as 100 knots as much as 10 miles ahead of the storm. The downburst is a really intense localized downdraft flowing out of a thunderstorm. The power of the downburst can exceed aircraft climb capabilities. The downburst (tright here are 2 types of downbursts: macrobursts and microbursts) normally is a lot closer to the thunderstorm than the gust front. Dust clouds, roll clouds, intense rainloss or virga (rain that evapoprices before it reaches the ground) are because of the opportunity of downburst task yet there is no means to accurately predict its event.

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Temperature Inversions. Overnight cooling creates a temperature invariation a couple of hundred feet above the ground that have the right to create substantial wind shear, specifically if the inversion is coupled with the low-level jet stream.

As a nocturnal invariation develops, the wind shear close to the peak of the invariation rises. It typically reaches its maximum rate shortly after midnight and also decreases in the morning as daytime heating dissipates the inversion. This phenomenon is known as the low-level nocturnal jet stream. The low level jet stream is a sheet of solid winds, countless miles long, numerous miles wide and also hundreds of feet thick that forms over level terrain such as the prairies. Wind speeds of 40 knots are widespread, however better speeds have actually been measured. Low level jet streams are responsible for hazardous low level shear.

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As the invariation dissipates in the morning, the shear plane and also gusty winds move closer to the ground, leading to windshifts and also increases in wind speed close to the surchallenge.

Surconfront Obstructions. The ircontinuous and also turbulent circulation of air approximately mountains and hills and through mountain passes causes major wind shear difficulties for aircraft approaching to land also at airports close to mountain ridges. Wind shear is a phenomenon associated through the mountain wave. Such shear is virtually totally unpredictable yet should be supposed whenever before surchallenge winds are solid.

Wind shear is likewise associated through hangars and large buildings at airports. As the air flows approximately such large structures, wind direction changes and also wind rate rises bring about shear.

Wind shear occurs both horizontally and also vertically. Vertical shear is the majority of widespread close to the ground and have the right to pose a serious peril to airplanes during take-off and also landing. The airplane is flying at lower speeds and also in a reasonably high drag configuration. Tright here is little altitude available for reextending and also stall and also maneuver margins are at their lowest. An aircraft encountering the wind shear phenomenon may endure a huge loss of airrate bereason of the sudden adjust in the relative airflow as the airplane flies right into a brand-new, moving air mass. The abrupt drop in airspeed might lead to a stall, developing a dangerous instance when the plane is just a few hundred feet off the ground and also very fragile.

THE JET STREAM

Narrowhead bands of exceedingly high rate winds are well-known to exist in the greater levels of the environment at altitudes ranging from 20,000 to 40,000 feet or more. They are well-known as jet streams. As many kind of as 3 significant jet streams may traverse the North American continent at any kind of provided time. One lies across Northern Canada and one throughout the UNITED STATE A third jet stream may be as much south as the northern tropics however it is rather rare. A jet stream in the mid latitudes is mostly the strongest.

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The jet stream appears to be very closely associated with the tropopausage and also with the polar front. It typically creates in the break in between the polar and also the tropical tropopausage wright here the temperature gradients are intensified. The expect position of the jet stream shears south in winter and north in summer via the seasonal migration of the polar front. Due to the fact that the troposphere is deeper in summer than in winter, the tropopausage and also the jets will nominally be at higher altitudes in the summer.

Long, strong jet streams are normally also connected through well-emerged surface lows beneath deep top troughs and also lows. A low developing in the wave along the frontal surconfront lies south of the jet. As it deepens, the low moves close to the jet. As it occludes, the low moves north of the jet, which crosses the frontal mechanism, near the point of occlusion. The jet flows approximately parallel to the front. The subtropical jet stream is not linked with fronts yet develops bereason of solid solar heating in the equatorial regions. The ascfinishing air transforms poleward at extremely high levels however is deflected by the Coriolis pressure into a solid westerly jet. The subtropical jet predominates in winter.

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The jet streams circulation from west to east and may encircle the entire hemispbelow. More regularly, bereason they are stronger in some locations than in others, they break up right into segments some 1000 to 3000 nautical miles long. They are generally around 300 nautical miles wide and may be 3000 to 7000 feet thick. These jet stream segments relocate in an easterly direction adhering to the motion of pressure ridges and also troughs in the upper setting.

Winds in the central core of the jet stream are the strongest and also may reach speeds as great as 250 knots, although they are mostly between 100 and also 150 knots. Wind speeds decrease towards the outer edges of the jet stream and also might be blowing at only 25 knots there. The rate of decrease of wind rate is significantly higher on the north edge than on the southerly edge. Wind speeds in the jet stream are, on average, substantially more powerful in winter than in summer.

Clear Air Turbulence. The many probable location to expect Clear Air Turbulence (CAT) is just over the main core of the jet stream close to the polar tropopause and also simply listed below the core. Clear air disturbance does not happen in the core. CAT is encountered more typically in winter when the jet stream winds are strongest. Nevertheless, CAT is not always present in the jet stream and also, because it is random and transient in nature, it is nearly impossible to forecast.

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Clear air turbulence may be connected via other derekwadsworth.com patterns, particularly in wind shear associated with the sharply curved contours of solid lows, troughs and ridges aloft, at or below the tropopause, and also in locations of solid cold or heat air advection. Mountain waves create severe CAT that may extfinish from the mountain crests to as high as 5000 feet over the tropopausage. Due to the fact that major CAT does pose a danger to airplanes, pilots should attempt to stop or minimize encounters through it. These rules of thumb might help avoid jet streams via solid winds (150 knots) at the core. Strong wind shears are likely over and listed below the core. CAT within the jet stream is even more intense over and also to the lee of hill varieties. If the 20-knot isotachs (lines joining areas of equal wind speeds) are closer than 60 nautical miles on the charts mirroring the locations of the jet stream, wind shear and also CAT are possible.

Curving jet streams are most likely to have turbulent edges, particularly those that curve roughly a deep push tturbulent. When modeprice or severe CAT has actually been reported or is foreactors, readjust speed to rough air speed automatically on encountering the first bumpiness or also prior to encountering it to protect against structural damages to the aircraft.

The locations of CAT are generally shenable and also narrowhead and elongated with the wind. If jet stream disturbance is encountered through a tail wind or head wind, a turn to the ideal will discover smovarious other air and also more favorable winds. If the CAT is encountered in a crosswind, it is not so essential to readjust course as the rough location will certainly be narrowhead.