Answer:
When a parcel of air rises up the side of a mountain, it cools as it ascends due to adiabatic processes. The rate of cooling depends on whether the air is saturated (reached its dew point) or unsaturated. Let's calculate the temperatures at different altitudes:
1. At 1000 meters:
- The air parcel is still unsaturated because it hasn't reached the dew point.
- The dry adiabatic lapse rate is about 9.8°C per 1000 meters of ascent.
- Starting temperature at 0 meters = 25°C
- Temperature at 1000 meters (unsaturated) = 25°C - (1 * 9.8°C) = 25°C - 9.8°C = 15.2°C
2. At 2000 meters:
- The air parcel is still unsaturated.
- Using the dry adiabatic lapse rate, the temperature at 2000 meters can be estimated.
- Starting temperature at 0 meters = 25°C
- Temperature at 2000 meters (unsaturated) = 25°C - (2 * 9.8°C) = 25°C - 19.6°C = 5.4°C
3. At 3000 meters:
- The air parcel reaches its dew point, becoming saturated. Beyond this point, we use the moist adiabatic lapse rate, which is about 5°C per 1000 meters.
- Starting temperature at 2000 meters = 5.4°C
- Temperature at 3000 meters (saturated) = 5.4°C - (1 * 5°C) = 0.4°C
4. Cloud formation typically occurs when air becomes saturated, which in this case happens at 3000 meters when the temperature reaches the dew point. So, cloud formation occurs at 3000 meters in this scenario.
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