<P> Whereas the ITCZ has a global extent, South America is subject to its own unique climate patterns . which have been organised into the South American Monsoon System (SAMS). As an integrated component in the global climate system, the SAMS is influenced the Atlantic sector of the ITCZ, variability in the adjacent Pacific and Atlantic Oceans, the Andean and central - east Brazil topography, complex land surface processes and relations with land use change, and interactions involving topography and soil moisture . The SAMS framework comprises several distinct subcomponents, which are discussed below: </P> <Ul> <Li> The Pacific and Atlantic subtropical high: These are semi-permanent high pressure systems caused by descending sectors of the equatorial Hadley cells . The air masses are relatively warm and dry, and move in an anticyclonic circulation pattern over the sub-tropical oceans . The Pacific High is generally stable, whereas the Atlantic High moves throughout the year . During the summer, it covers most of the midlatitude and subtropical Atlantic Ocean . During winter, it is smaller and moves to the east . </Li> <Li> The Gran Chaco thermal low: A semi-permanent thermal - orographic depression located over the slope extending from Chaco to the Los Andes mountain range in the Argentine Northwest . It can be considered, together with the Bolivian High, as the regional response of the tropospheric circulation to the strong convective heating over the Amazon--central Brazil . The Andes effect reinforces the strength of the Chaco Low as an orographic barrier . It is present throughout the year, but is more intense during the summer, with a strong thermal component caused by the combination of high insolation and dry surface conditions . The resulting pressure gradient between the south Atlantic subtropical high and the Chaco low forces the easterly winds over the Amazon basin to turn southward, being channelled between the eastern slope of the Andes and the Brazilian Plateau . </Li> <Li> The South Atlantic Convergence Zone (SACZ): The SACZ controls rainfall in the southern subtropics and extends southeastward from the large continental convective zone of tropical South America . It is generated by moisture convergence between the South Atlantic high pressure zone and the continental thermal low pressure zone . The location of the SACZ is influenced by the topography in central - east Brazil Vera et al. (2006). The intensity of the SACZ is highest in austral summer, in phase with intensifying continental heating and convection . Weak SACZ is accompanied by enhanced rainfall over northern Argentina and southern Brazil . These positive rainfall anomalies are supported by a strong southward moisture flux at about 35 ° S--60 ° W that shifts eastward to about 40 ° W for the opposite phase of the seesaw, in accordance with an eastward displacement of the Atlantic high . An intensified SACZ is associated with enhanced streamflows to the north and diminished flows to the south . This north--south separation is probably related to the anomalously warm sea surface temperatures (SSTs) over the tropical and subtropical South Atlantic that strengthens the low - level meridional temperature gradient, intensifying the South Atlantic High and consequently the trade - winds . </Li> <Li> Polar outbreaks: Polar outbreaks occur when cold dense polar air masses pass beneath warmer tropical air masses, significantly cooling subtropical South America . They occur as a result of anticyclogenesis in the Pacific subtropical high, which is constrained at a low level by the southern extent of the Andes mountain range . This leads to the formation of a slow - moving long wave that creates mountain - parallel, ageostrophic flow, causing incursions of high - latitude cold air . They generate an important drop in temperature and increase in pressure, resulting in regional precipitation for southern South America . These surges occur mainly during the winter but their impact on the precipitation is even greater during summer . </Li> <Li> Low Level Jet (LLJ): LLJs originate in a low pressure area over the northern Andes and provide moisture for subtropical latitudes . During summer, they operate as localised wind maximum within the lower 1--2 km of the atmosphere, channelled by the Andes, terminating in southeastern South America . They are controlled by Amazonian wind patterns, which are influenced and controlled by patterns of insolation . They transport large amounts of moisture from the Amazon basin to the monsoonal anitcyclone over Bolivia . A suppressed SACZ and increased convection in the sub-tropical plains is associated with a strengthening of the LLJ . These phases are linked to short - term extreme precipitation events in the plains of central Argentina . When the LLJ is weak, there is enhanced SACZ and suppressed convection to the south and extreme heat waves over the sub-tropical regions . It also generates turbulence through shear and participates actively as trigging mechanism for the formation of severe storm and Mesoscale Convective Systems over Paraguay, Northern Argentina and South of Brazil . </Li> <Li> Westerlies: South America experiences westerly winds in the middle latitudes, caused by the Coriolis force and associated geostrophic circulation patterns . They are more intense than their Northern Hemisphere counterparts due to the lack of continental landmass in the Southern Hemisphere . They reach their maximum speed in the troposphere, where they form jetstreams . In particular, over the southern tip of South America and the adjacent south Pacific, the westerlies are strongest during austral summer, peaking between 45 ° and 55 ° S. During the austral winter, the jetstream moves into subtropical latitudes (its axis is at about 30 ° S) and the low - level westerlies expand equatorward but weaken, particularly at ~ 50 ° S . The pressure gradients between the polar low - pressure belt and the Pacific high - pressure cell, combined with these westerlies, results in permanent anticyclogenesis . Northward penetration of atmospheric perturbations from the westerlies is possible when the southeast Pacific anticyclone is weakened or moves equatorward, allowing penetration of westerly storm tracks to latitudes as far north as 31 ◦ S. In the Andes, winter rains reach further north . During summer, the Pacific anticyclone shifts southward, impeding the northward migration of the westerlies . </Li> <Li> The Bolivian High: large anticyclonic circulation centred near 15 ° S, 65 ° W. It has been explained as the response of diabatic local heating in the Amazon region . The SACZ has a strong influence on the position and intensity of the Bolivian High </Li> <Li> The Madden--Julian oscillation (MJO): The MJO is characterized by an eastward progression of large regions of both enhanced and suppressed tropical rainfall, observed mainly over the Indian Ocean and Pacific Ocean . It is a source of intra-seasonal variability affecting South America that seems to be related to a combination of tropical circulation changes and midlatitude Rossby wave trains that propagate into South America . </Li> </Ul> <Li> The Pacific and Atlantic subtropical high: These are semi-permanent high pressure systems caused by descending sectors of the equatorial Hadley cells . The air masses are relatively warm and dry, and move in an anticyclonic circulation pattern over the sub-tropical oceans . The Pacific High is generally stable, whereas the Atlantic High moves throughout the year . During the summer, it covers most of the midlatitude and subtropical Atlantic Ocean . During winter, it is smaller and moves to the east . </Li> <Li> The Gran Chaco thermal low: A semi-permanent thermal - orographic depression located over the slope extending from Chaco to the Los Andes mountain range in the Argentine Northwest . It can be considered, together with the Bolivian High, as the regional response of the tropospheric circulation to the strong convective heating over the Amazon--central Brazil . The Andes effect reinforces the strength of the Chaco Low as an orographic barrier . It is present throughout the year, but is more intense during the summer, with a strong thermal component caused by the combination of high insolation and dry surface conditions . The resulting pressure gradient between the south Atlantic subtropical high and the Chaco low forces the easterly winds over the Amazon basin to turn southward, being channelled between the eastern slope of the Andes and the Brazilian Plateau . </Li>

How do location and landforms affect latin americas climate regions