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HYDROMETEROLOGY (LESSON 1..6B)

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HYDROMETEROLOGY (LESSON 1..6B)

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WIND AND ITS HYDROLOGIC IMPLICATIONS

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Grace Balahay
Grace Balahay
United States

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HYDROMETEROLOGY (LESSON 1..6B)
 

HYDROMETEROLOGY (LESSON 1..6B)Online version

WIND AND ITS HYDROLOGIC IMPLICATIONS

by Grace Balahay
1

Air in motion

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2

It is a natural phenomenon that is influenced by a variety of factors, including the Earth's rotation, temperature gradients, and the composition and structure of the atmosphere.

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3

from which the wind is blowing

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4

the wind doesn't flow directly from high to low pressure but gets deflected to the right in the Northern Hemisphere and to the left in the Southern Hemisphere.

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5

Winds tend to blow from the cooler bodies of water toward the warmer land

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6

Mountains radiate heat at night, this makes the mountains cool. At this time the valley is relatively warm. As a result, cold and heavy winds blow down the mountain. The wind that blows at night towards the bottom of the valley is known as

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7

During the day the mountains are warmer than the bottom of the valley. This causes high pressure at the bottom of the valley and low pressure at the side of the mountain. For this reason, the wind that blows upwards through the mountain during the day is called

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8

Lower layer of the atmosphere where wind speeds are reduced and direction are deflected because of friction produced by trees, buildings, and other obstacles.

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9

lower part of the atmosphere directly influenced by its contact with a planetary surface. • extends from the ground up to a height where atmospheric properties like temperature, moisture, and wind speed become relatively constant with height.

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10

(0-1 cm), molecular transport, no turbulence

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11

(0-100 m), strong gradients, very vigorous turbelence

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12

(100m -1 km), well-mixed, vigorous turbulence

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13

inversion, intermittent turbulence

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14

refers to a change in wind speed or direction with height in the atmosphere. It can occur either vertically or horizontally

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15

upward energy transport

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16

Strong winds combined with low temperatures can result in lower effective temperatures, known as the

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17

Refers to the change in temperature with respect to the altitude of an air parcel. Usually focuses on the troposphere due to its impact on the weather

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18

Refers to the change in temperature with respect to the altitude of an air parcel without gaining or losing any heat to the environment surrounding the parcel

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19

6.5 °C/km (or K/km)

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20

Unsaturated air parcels cools ~9.8 °C/km (or K/km)

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21

• Saturated air parcels cools ~3-6 °C/km (or K/km) • Occurs when the air parcels reached dewpoint temp.

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22

Equal temperatures are referred to as

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23

is determined by raising or lowering this hypothetical air parcel and comparing its properties to those of the surrounding environment.

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24

If a rising air parcel has a lower temperature than the surrounding environment, the rising parcel is denser, and will tend to sink. In this case, the atmosphere is said to be

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25

If a rising air parcel has a higher temperature than the surrounding environment, the rising parcel is less dense, and will continue to rise. In this case, the atmosphere is said to be

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26

vertical motion is suppressed, and a displaced parcel will move back toward its original position.

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27

air parcels displaced either upward or downward will continue in that direction

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