2. Atmospheric Moisture Lapse Rate By K. Y. NG

3. 105 Temp. °C 0-5-10 -15 2000 1500 1000 500 Height (m) CondensationLevelDALR  10°C /  1000 m SALR  5°C /  1000 m Dry Adiabatic Lapse Rate & Saturated Adiabatic Lapse Rate 500m: 5°C 2000m: -2.5°C

4. 105 Temp. °C 0-5-10 -15 2000 1500 1000 500 Height (m) Stability ELR (1)  4°C /  1000m SALR DALRCondensationLevel 2000m: 2°C 2000m: -2.5°C Rising air parcel is colder than surrounding air (-2.5 °C < 2 °C). The air parcel sinks back to its starting point, i.e. STABILITY ELR (1) < SALR < DALR

5. 105 Temp. °C 0-5-10 -15 2000 1500 1000 500 Height (m) Instability ELR (2)  12°C /  1000m SALR DALRCondensationLevel 2000m: -14°C 2000m: -2.5°C Rising air parcel is warmer than surrounding air (-2.5 °C > -14 °C). The air parcel will rise continuously, i.e. INSTABILITY ELR (2) > DALR >SALR

6. 105 Temp. °C 0-5-10 -15 2000 1500 1000 500 Height (m) ELR (3)  8°C /  1000m SALR DALRCondensationLevel 2000m: -6°C 2000m: -2.5°C Below 850m, as the air parcel is cooler than the surrounding air (DALR & SALR > ELR (3) ), the air parcel will sink normally, i.e. stable air. IF the air parcel is forced to rise above 850m, it will be warmer than the surrounding air (SALR < ELR (3) ). The air parcel will rise continuously, i.e. unstable air. 850m Conditional Instability UNSTABLE AIR STABLE AIR CONDITIONAL INSTABILITY

7. Conclusion THE END