The southeast Brazilian passive margin records a long history of tectonic magmatism events since the Late Jurassic. Those events were consequence of the South Atlantic Ocean [1] [2] . The continental breakup preceded by intense tholeiitic magmatism in south and southeast of Brazil, with magmatic climax at 132 Ma [3] .

After the rifting process has ceased, an epeirogenic uplift of the continental crust has started in response to the drifting of the South American Platform over a thermal anomaly that accompanied an intense alkaline and basaltic magmatism [4] . This alkaline volcanism from the Late Cretaceous generates a very particular structure on the Brazilian southeast named Poços de Caldas Alkaline Massif (PCAM). The structure covers over 800 km² [5] and it is the greatest from the set of intrusions that form the Poços de Caldas-Cabo Frio Lineament [6] . The Poços de Caldas massif is mainly constituted by subvolcanicphonolites (tinguaites), nephelinesyenites (NeS), and mostly altered volcanic phonolites, in part enclosing the overlying eolian Botucatu sandstones and some Serra Geraldiabases [7] [8] .

The topography is characterized by dissected plateau with irregular topographic ridges and peaks with elevations between 900 and 1300 m (a.s.l.) on the metamorphic basement and from 1300 to 1700 m (a.s.l.) on the PCAM region. The geomorphological development of most part of the highlands on southeast of Brazil was explained by the [9] pediplanation scheme or by the correlation between the pediplanation with favourable climatic conditions and intermittent uplift and dissection [10] . Accoording to these concepts erosional surfaces were recognized in the area nevertheless, there are different point of views about the age, origin and structure. In these sense the main objective of this work was to present information about the summit heights in the area and try to associate with palaeosurfaces using techniques that allows identifying the process that is controlling the landscape evolution in the region.

Some geomorphic indices have been developed to identify areas experiencing rapid tectonic deformation [11] [12] . Geomorphic indices are particularly useful in tectonic studies because they provide a rapid evaluation of large areas and can be obtained easily from topographic maps or aerial photos [13] . Moreover, in recent decades, the increasing usefulness of GIS software has made it easier to undertake quick and detailed processing of data [14] . The Stream Length-Gradient Index (SL Index) is one of the quantitative geomorphic parameters included in morphotectonic investigation. In the regional scale of analysis, the SL Index can be a useful tool to detect tectonic displacements and reactivation [15] . The longitudinal profile of a channel determines the gradient of a river and their behavior along the channel from the headwater to mouth [16] .

The present study sets out to better understand the configuration of the long-term landscape evolution of the Poços de Caldas Alkaline Massif that is part of the southeast Brazilian highlands, providing insights on the behaviour of the coupled magmatic tectonic-erosional system.

The Poços de Caldas Plateau (PCP) is located in the southeast part of Brazilian highlands in the limit between São Paulo and Minas Gerais states and on northwest of Rio de Janeiro State. As described in [17] , this is plateau as a small morphostructural unit represented by a high land relief, with a circular configuration. The highest part (above 1400 m) of the plateau is the Poços de Caldas Alkaline Massif (PCAM) structure and the lower part (between 900 and 1400 m) is part of the metamorphic basement called North Crystalline Zone (NCZ). The PCP emplaced in the Guaxupé-Socorro Nappe is limited on north by the São Francisco Cráton, on south an east by the RibeiraOrogenic Belt and west by the Paraná Basin.

The area is located in the Mantiqueira Geological Province context, which is an orogenic system parallel to the south Atlantic coast on southeast and south of Brazil developed in the Brazilian orogeny cycle [18] . The Mantiqueira Province is a large, complex structural province deformed by the Neoproterozoic/Early Paleozoic BrasilianoOrogenic event in South America, related to the Pan-African orogeny. The central part of the province, is formed by the Brasilia SulOrogen, RibeiraOrogen and the interference zone between the Apiaí, São Roque and Embu terrains, that was originated from a sequence of collisions from the 630 to 510 Ma [19] . The map on Figure 1 illustrates the location of the study area located in the Brasilia Sul belt delimited by the São Francisco craton, Parana Basin and Ribeira belt.

The PCAM is located in the nappe system in south-southwest São Francisco Craton. Represents the southern extension of the Brazilian belt and describes an inverted metamorphic pile (stack) of green schist facies (bottom) toward amphibolite facies (Carmo da Cachoeira e Aiuruoca-Andrelândianappes) and high pressure granulites in the top, under a high temperature allochtonous (Socorro-Guaxupénappe).

The Guaxupé-Socorro Nappe has a very complex intrusive and metamorphic history and was attached to the

southernmost portion of the Brasília Belt and later transported during the Neoproterozoic over the São Francisco Craton in an east direction. Two possibly related segments are recognized in the Nappe, the northernmost triangular Guaxupé block, with its base covered by sediments of the Paraná Basin, and the southern structure, Socorro [20] [21] . Several Archean to Proterozoiuc units were recognized within the Guaxupé block: the complexes Caconde (supracrustal quartz gneisses), Alfenas-Guaxupé (assorted granulites of igneous origin), Varginha (high-grade gneisses and paragranulites) and Pinhal (migmatitic and deformed granite facies) [22] .

The basement areas that constitute the Guaxupé block and the surrounding regions are cut by several linear features interpreted mostly as old reactivated faults. The predominant fault direction is NE and NW, parallel to the two most commonly observed structural trends in the basement of southern and SE Brazil. Observation on a regional scale show an increase in the amount of the NE and NW fractures in the region around PCAM. As well as an arching of structural trends in the basement rocks, to the east, thus creating a zone of weakness that may have channelled the flow of the PCAM magmas [23] . The emplacement of the PCAM was controlled by the passage of the Trindade plume, farther north, which may have been deflected to the south by the deep keel of old and cold cratonic areas, such as the Sao Francisco craton, generating magmas that upsurge into the surface along deep pre-existing structures [6] -[24] .

This event formed the Poços de Caldas-Cabo Frio Magmatic Lineament, as defined by [25] , is a WNW-ESE structural feature, 60 km wide by 1150 km long, developed from Jaboticabal (Northern Sao Paulo State) eastwards, up to the Almirante Saldanha Bank, region of the boundary between continental and oceanic crusts. Indeed, the topographic and lithologic features, shows prominent tinguaite ridges that suggest that the massif represents the upper part of a caldera-like structure, with early appearance of tinguaites as ring dikes, followed by collapse and the intrusion of the inner tinguaites and some outpouring of phonolites, culminating with the late intrusion of most nephelinesyenites [7] [8] .

Geologic observations on the alkaline massif show that the miaskitic-intermediate nephelinesyenites are somewhat older than the more evolved agpaitic varieties. Many elongated nephelinesyenite bodies are confined to the rim areas, a preferred site for the intrusion of these magmas and an indirect evidence for the existence of “ring structures”; the northern-rim fluorite-bearing grey nephelinesyenite is clearly an incomplete ring dike [5] . In addition, it can be found in some areas of the massif, isolate sediment bodies surrounded by neighbourphonolitic rocks with intrusive contact and ramdom strikes and dips. They were correlated to the Botucatu Fomation by [26] and [7] , which suggested a simultaneous deposition with the alkaline pyroclastic rocks and a general dip minor than 20 degrees to the centre of the alkaline complex to justify the caldera collapse. Figure 2 is showing the main geological setting of the area.

The analysis of Geomorphic Indexes of drainage systems allows detecting recent tectonic activity and uplifting [26] as river channels are very sensitive to changes in the parameters that control their shape and gradient [27] - [29] . Rivers tend to develop equilibrium profiles in relative short times, and consequently, anomalies in the river network systems, can be considered recent tectonic activity in case e other factors as lithology or climate are discarded [30] . Two geomorphic indexes were used in this paper the River Longitudinal Profiles and the Slope Gradiente Index (SL). These techniques are used to identify areas experiencing rapid tectonic deformation [11] [12] . Geological and topographic maps were also analysed in order to delineate areas of accordant summit heights.

The topographic map on Figure 3 shows the summit levels from the region. According to [36] the concentration of summit heights in certain heights correspond with the scheme of surfaces, pediments and terraces proposed by [39] [40] . Four topographic levels were defined ranging from <900 to >1500 m of elevation. The differences in elevation in the lower levels appear to be mostly due to differential weathering and erosion. However the upper intermediate level (900 - 1200 m) shows that part of the metamorphic basement is in the same level as the alkaline rocks of PCAM. The upper level is formed by the top of the circular structures of the PCAM and the MaciçoPedraBranca on SE. This level is supposed to have been formed before the breakup of the Gondwana continent according with [9] , although this level was formed after the PCAM intrusion, which means they cannot be older than 80 Ma. It is possible to see that this is just one of the several limitations in using only the

summit heights as evidence of erosional surfaces as postulated by [9] .

The drainage network of the region is distributed in several ways, the main types are dendritic, parallel, trellis and rectangular. In the areas close to the alkaline massif lies annular drainage pattern. All this different drainage patterns means several types of controls like lithology, structure and topography. The SL Index where calculated for the main stream of the rivers and where interpolated on the map (Figure 4). The results show that most of the rivers are controlled by the intense pattern of NW-SE, NE-SW e NNE-SSW trending faults that can also be seen in the longitudinal profile of the main rivers.

According to [41] , the E-W and ENE-WSW lineaments are very evident in the area and they related them to the OuroFino-Jacutinga shear zone in the south part of the study area (Figure 5). In addition, the directions WNW-ESE are very common and are related to the Campo do Meio shear zone on the northern part of the area. N-S and NW-SE lineament directions are also very abundant in the region and the authors attribute them to Cenozoic tectonic movements, however part of them are related to the Pre-Cambrian structures. The lineament relative frequency suggests two main tectonic moving directions that are expressed on the NE-SW and NW-SE morphology. The N-S and ENE-WSW directions cross the PCAM and are related to Upper and Upper Intermediate levels indicating also Cenozoic movements (Figure 6) [42] . Areas characterized by pronounced accordant summit heights are associated with highly dissected terrains and the low and moderate SL Index corresponds with streams with few knickpoints that are adjusted to the major rivers (Figure 8). However, this is not applied by the Machado (1), Peixe (2), Pardo (3) and Taquari (6) rivers as they are cut by these faults in several parts of the main stream.

The longitudinal profiles from NCZ show the fault controls over the main rivers. The SL Index curve shows that the highest values coincide with the knickpoints regression. Those anomalies are attributed to the structure that cut the river segments in several parts from the upper to the lower course. On the other hand Antastiver in PCAM does not present the same pattern as the course is following the structures and not being cut by them. The Antas River cross the ring structure of PCAM on the north shows that it was installed after the cooling of the massif. The Peixe River longitudinal profile (Figure 6, n. 2) shows several knickpoints coinciding with the highest SL Index values. Those values are related to the NW-SE faults that are perpendicular to the main stream. Peixe River is located in the NCZ and is related to the Lower Intermediate and Lower Levels defined in Figure 3. Pardo River is the greatest in the region serving as regional base level (except Machado e Peixe River that are

also tributaries of the Rio Grande drainage basin). The SL Index highest values coincide with the knickpoints on the longitudinal profile (Figure 6, n. 3). The river belongs to the NCZ and the main stream cross the levels Upper Intermediate, Lower Intemediate and the Lower. This river crosses the Paraná Basin in the west side of the region, although in this work it was considered just the upper course that belongs to the crystalline basement.

Machado River is a drainage basin that deserves some special attention, as the main stream has distinct morphologies. From the upper to middle course it flows from on a smooth plateau with about 1250 m high (average) and present characteristics like wide and open valley, suspended sediment, several meanders and abandoned meanders, it runs from the south to the nor-northwest until the middle point where it fits on a fault lineament with SW-NE direction.

From this point the river morphology changes into a bedrock channel, forming a V-shaped valley. These characteristics remain about 20 km when the channel starts to present a meandering morphology until reaches the mouth. All this features are indicating an inversion of the drainage that probably was running to the south and in some moment starts running to north and northeast. This change in the river direction was associated with a drainage capture [41] . The Longitudinal Profile of Machado River shows this drastic change in elevation (400 m), where the SL Index value is the highest comparing with the all other river values. The upper course belongs to the upper intermediate level while the lower course flows over the lower level.

The structures cutting the upper course are not influencing the dynamic of river channel. Figure 7 calls attention for the Machado River longitudinal profile, each letter A, B and C represents one of yours segments as follows, Upper course, Medium course and Lower course. The pictures in Figure 8 show the differences on the river morphology in each part of its course, indicating an inversion of the river direction, probably from N-S to a S-N/SW-NE, caused by a river capture. [43] had already called attention for the behaviour of the Machado River and also applying morphometric analysis for the whole drainage basin, showing that it is controlled part for the lithology and part for the structural lineaments. The authors also suggest a change in the course, but there are not enough tools to affirm.

All these topography and drainage patterns, that are very common in southeastern Brazil, are providing evidence of recent uplift, block-faulting, and river capture, all of which are symptomatic of active tectonics [44] . Although, the morphometric analysis shows that the main river basins are controlled by fault lineaments, apatite fission track ages shows that most of them should have been reactivated on the Early Cretaceous and specially the Late Cretaceous and Palaeogene events [42] [45] -[47] . After that the climate changes, as the transitional wet- dry periods of the Quaternary, is controlling the rivers and the landscape in general, the same way it is controlling great part of the southeast Brazilian highlands as in Serra do Mar and Mantiqueira Mountain Range [48] - [51] .

According to [36] summit levels and accordant summit heights are often interpreted as remnants of formerly more extensive denudation surfaces that have been formed by pediplanation or processes related to etchplanation. In Poços de Caldas Plateau summit levels and accordant summit heights have been interpreted as remnants of uplifted planation surfaces that correspond with denudation surfaces in the hinterland [9] -[17] ; However the Late-Cretaceous and Paleogene ages obtained in this area shows that the surface in the upper area cannot be older, which proving that there are several limitations to use just the summit heights as evidence of dissected palaeo-surfaces [43] [52] . The thermochronological data is not supporting the Gondwana surface on the top [42] [45] -[47] . More data is needed to confirm the existence of those erosional surfaces in the area.

The SL Index from this area is highest comparing to the others, especially on the medium course of Machado River where it fits on a NE-SW fault that is probably related to the reactivation to the Ouro-Fino-Jacutinga shear zone. The morphometric analyses show that after the reactivation of the shear zones in the Triassic, there was a surface uplift, and a change on the river base level from the south to the north. The main rivers at that time like the Machado and Pardo start to adapt to the new structures and run to the north and northwest. The South Atlantic Opening reactivated the old faults in the area and generated new ones (NE-SW) adjusting once again the old rivers, especially on the lower intermediate level (where the AFT ages are from this period). Most of these structures are responsible for elevating the SL Indexes in those rivers. The drainage in PCAM was set up after the continental rift tectonic event in the beginning of Paleocene, explaining the low SL Index as the rivers are not being cut by the structures but they are installed inside the valleys formed by them.

The research was supported by Coordenação de Aperfeiçoamento de Pessoal de Nível Superior (CAPES). We especially thank Ana OlíviaBarufi Franco-Magalhães (UNIFAL, Poços de Caldas-MG) for the motivation and encouragement for writing this paper.