Geography Reference
In-Depth Information
Fig. 7.13 Annual cycles' domain-averaged in the years 2090-2100 between 49 and 638W and
128S-28N. All flux is in W/m
2
, surface temperature inC, precipitation in mm. Solid line is the
control simulation, and the dashed line is deforestation simulation
The spatial distribution of differences in surface temperature between the
control test and sensitivity test is significantly influenced by the forest land
changes. Obviously, the surface temperature increases over the western region,
associated with the reduction of precipitation and soil moisture that will reduce the
latent heat flux discharge from the land surface into atmosphere. Massive defor-
ested areas experience a significant increase of temperature and decrease of pre-
cipitation. In addition, deforestation will intensify the precipitation shift by
increasing its amount in the southeast region and even further, and decreasing the
precipitation in the northwest region (Fig.
7.14
). The precipitation variability can
be explained by that deforestation may influence the propagation of squall lines,
which will reduce the water supply in these regions. Meanwhile, the convection
and speed effects will also impose a negative feedback in these regions.
To study the spatial heterogeneity of these climatic metrics in longitude and
latitude direction, the average surface temperature and precipitation in different
zones were calculated (Fig.
7.14
, down panels). Apparently, the surface temper-
ature fluctuates dramatically in the western region and almost remains stable in the
eastern part, which means that the surface temperature has a longitudinal distri-
bution characteristic. Meanwhile, the zonally average temperature of north region
increases most greatly by 0.0350 C in year 2100 induced by deforestation, while
