This is the author's post-print and is released with a Creative Commons Attribution Non-Commercial No Derivatives License.The definitive published version is available from Elsevier via http://dx.doi.org/10.1016/j.gexplo.2015.03.007\ud © 2015 Elsevier B.V. All rights reservedThe mode of occurrence, mobility and fractionation of REE have been investigated in the geochemical\ud context of the Serra Dourada Granite, an A-type granitic body located in northern Goi´as State, Brazil.\ud Several analyses were performed to best characterize each mode of occurrence of REE, from fresh rock\ud to its products of alteration such as the saprolite, placers and clayish horizon. In the fresh rock it was\ud found that the REE budget is related to monazite-(Ce), xenotime-(Y), bastn¨asite and allanite. Resistant\ud monazite-(Ce) and xenotime-(Y) withstand fluvial transportation and are concentrated in placers whithin\ud the massif, whereas bastn¨asite and allanite do not. The alluvial sediments contain up to 0.87wt%\ud monazite-(Ce) and 0.46wt% xenotime-(Y). Considering only the heavy minerals, monazite-(Ce), zircon\ud and ilmenite represent 60-80% of the total variability, being monazite-(Ce) and xenotime-(Y) the most\ud important REE carriers. The same minerals are also present, although in lower amounts, in the saprolite.\ud Both qualitative and quantitative electron probe microanalysis were carried out in detrital monazite-\ud (Ce) and xenotime-(Y) to assess their main features and composition. Monazite-(Ce) REE contents are\ud 60wt% in average, whilst REE contents in detrital xenotime-(Y) are 55 wt% in average. Low totals are\ud ascribed to the alteration of the minerals caused by the presence of both organic and inorganic ligands\ud present in the system. The results support the idea that REE are mobile under supergene conditions\ud and during granite weathering, tending to be higher and more fractionated towards the products of\ud alteration (saprolite, alluvial sediments and clayish horizon). REE2O3 contents in the fresh granite,\ud saprolite, alluvial sediments and clayish horizon are 0.07, 0.21, 1.2 and 0.11wt% respectively, the clayish\ud horizon being HREE-selective. Placer deposits and the clayish horizon tend to occur in low-slope areas\ud within the Massif, where deposition and accumulation is more favorable. The saprolite occurs preferably\ud in high-slope areas formed in situ at the expense of the granite. The placer deposits could be exploited,\ud but their occurrence is more restricted and local. The saprolite has the advantage of covering extensive\ud areas widely distributed over the granite. Currently a private company, the Serra Verde Mining, posses\ud the mining claims in the area to exploit the REE associated with the saprolite, under the model of\ud ion-adsorption type deposits

The Guaviare Complex is a new unit defined in the Colombian Amazonian Craton, which is part of the Precambrian basement located in southeastern Colombia. It is divided into three units according to their textural and compositional characteristics, termed Termales Gneiss, Unilla Amphibolite, and La Rompida Quartzite. Termales Gneiss rocks are petrographically classified as gneisses and quartz-feldspar granofels, with the local formation of blastomylonite-like dynamic rocks. The Unilla Amphibolite consists of only amphibolites, and La Rompida Quartzite consists of muscovite quartzites, quartz-feldspar granofels, and quartz-muscovite schists. The protoliths of Termales Gneiss and Unilla Amphibolite were formed in the Mesoproterozoic at 1.3 Ga due to bimodal magmatism (felsic and mafic) derived from mantle material, with some crust contamination that was probably related to the formation of extensional arcs associated with trans-arc basins in the NW section of the Amazon Craton. La Rompida Quartzite rocks originated from sediments derived from granite rocks and from other, older areas of the craton. These rocks have a maximum age of 1.28 Ga. The low-to-medium grade metamorphism that affected these units occurred from 1.28 to 0.6 Ga, most likely concurrently with the Putumayo orogeny of approximately 1.0 Ga, although it may have been an independent event.