<?xml version="1.0" encoding="UTF-8"?><xml><records><record><source-app name="Biblio" version="7.x">Drupal-Biblio</source-app><ref-type>17</ref-type><contributors><authors><author><style face="normal" font="default" size="100%">Soudani, K</style></author><author><style face="normal" font="default" size="100%">Hmimina, G</style></author><author><style face="normal" font="default" size="100%">Delpierre, N</style></author><author><style face="normal" font="default" size="100%">Pontailler, J.-Y.</style></author><author><style face="normal" font="default" size="100%">Aubinet, M</style></author><author><style face="normal" font="default" size="100%">Bonal, D</style></author><author><style face="normal" font="default" size="100%">Caquet, B</style></author><author><style face="normal" font="default" size="100%">de Grandcourt, A</style></author><author><style face="normal" font="default" size="100%">Burban, B</style></author><author><style face="normal" font="default" size="100%">Flechard, C</style></author><author><style face="normal" font="default" size="100%">Guyon, D</style></author><author><style face="normal" font="default" size="100%">GRANIER, a</style></author><author><style face="normal" font="default" size="100%">Gross, P</style></author><author><style face="normal" font="default" size="100%">Heinesh, B</style></author><author><style face="normal" font="default" size="100%">Longdoz, B</style></author><author><style face="normal" font="default" size="100%">Loustau, D</style></author><author><style face="normal" font="default" size="100%">Moureaux, C</style></author><author><style face="normal" font="default" size="100%">OURCIVAL, J.-M.</style></author><author><style face="normal" font="default" size="100%">Rambal, S</style></author><author><style face="normal" font="default" size="100%">Saint André, L</style></author><author><style face="normal" font="default" size="100%">Dufrêne, E</style></author></authors></contributors><titles><title><style face="normal" font="default" size="100%">Ground-based Network of NDVI measurements for tracking temporal dynamics of canopy structure and vegetation phenology in different biomes</style></title><secondary-title><style face="normal" font="default" size="100%">Remote Sensing of Environment</style></secondary-title></titles><keywords><keyword><style  face="normal" font="default" size="100%">Crops</style></keyword><keyword><style  face="normal" font="default" size="100%">Evergreen and deciduous forests</style></keyword><keyword><style  face="normal" font="default" size="100%">Ground-based NDVI</style></keyword><keyword><style  face="normal" font="default" size="100%">Herbaceous savanna</style></keyword><keyword><style  face="normal" font="default" size="100%">NDVI time-series</style></keyword><keyword><style  face="normal" font="default" size="100%">Phenology</style></keyword><keyword><style  face="normal" font="default" size="100%">Tropical rain forest</style></keyword></keywords><dates><year><style  face="normal" font="default" size="100%">2012</style></year></dates><publisher><style face="normal" font="default" size="100%">Elsevier Inc.</style></publisher><volume><style face="normal" font="default" size="100%">123</style></volume><pages><style face="normal" font="default" size="100%">234-245</style></pages><language><style face="normal" font="default" size="100%">eng</style></language><abstract><style face="normal" font="default" size="100%">Plant phenology characterises the seasonal cyclicity of biological events such as budburst, ﬂowering, fructiﬁ- cation, leaf senescence and leaf fall. These biological events are genetically pre-determined but also strongly modulated by climatic conditions, particularly temperature, daylength and water availability. Therefore, the timing of these events is considered as a good indicator of climate change impacts and as a key parameter for understanding and modelling vegetation–climate interactions. In situ observations, empirical or bioclimatic models and remotely sensed time-series data constitute the three possible ways for monitoring the timing of plant phenological events. Remote sensing has the advantage of being the only way of surface sampling at high temporal frequency and, in the case of satellite-based remote sensing, over large regions. Nevertheless, exogenous factors, particularly atmospheric conditions, lead to some uncertainties on the seasonal course of surface reﬂectance and cause bias in the identiﬁcation of vegetation phenological events. Since 2005, a network of forest and herbaceous sites has been equipped with laboratory made NDVI sensors to monitor the temporal dynamics of canopy structure and phenology at an intra-daily time step. In this study, we present recent results obtained in several contrasting biomes in France, French Guiana, Belgium and Congo. These sites represent a gradient of vegetation ecosystems: the main evergreen and deciduous forest ecosystems in temperate climate region, an evergreen tropical rain forest in French Guiana, an herbaceous savanna ecosystem in Congo, and a succession of three annual crops in Belgium. In this paper, (1) we provide an accurate description of the seasonal dynamics of vegetation cover in these different ecosystems (2) we identify the most relevant remotely sensed markers from NDVI time-series for determining the dates of the main phenological events that characterize these ecosystems and (3) we discuss the relationships between temporal canopy dynamics and climate factors. In addition to its importance for phenological studies, this ground-based Network of NDVI measurement provides data needed for the calibration and direct validation of satellite observations and products.</style></abstract></record><record><source-app name="Biblio" version="7.x">Drupal-Biblio</source-app><ref-type>17</ref-type><contributors><authors><author><style face="normal" font="default" size="100%">Cheddadi, Rachid</style></author><author><style face="normal" font="default" size="100%">Rossignol-Strick, M</style></author></authors></contributors><titles><title><style face="normal" font="default" size="100%">Eastern Mediterranean Quaternary paleoclimates from pollen and isotope records of marine cores in the Nile Cone Area</style></title><secondary-title><style face="normal" font="default" size="100%">Paleoceanography</style></secondary-title></titles><keywords><keyword><style  face="normal" font="default" size="100%">climate</style></keyword><keyword><style  face="normal" font="default" size="100%">Eastern Mediterranean</style></keyword><keyword><style  face="normal" font="default" size="100%">Evergreen and deciduous forests</style></keyword><keyword><style  face="normal" font="default" size="100%">isotopic stratigraphy (voyant)</style></keyword><keyword><style  face="normal" font="default" size="100%">pollen spectra</style></keyword></keywords><dates><year><style  face="normal" font="default" size="100%">1995</style></year></dates><volume><style face="normal" font="default" size="100%">10</style></volume><pages><style face="normal" font="default" size="100%">291-300</style></pages><language><style face="normal" font="default" size="100%">eng</style></language><abstract><style face="normal" font="default" size="100%">Pollen spectra from three eastern Mediterranean cores have been used to document the paleoclimates of the Levantine Basin borderlands over the last 250 kyr to establish the relationship between this regional climate data set and the global climate as recorded by foraminiferal δ18O and to compare it with proximal land pollen records. Core MD 84 642 with eight sapropels covers the last two climatic cycles up to the early Holocene, MD 84 627 with four sapropels goes back to 125 kyr, and MD 84 629 with one sapropel covers the last 70 kyr. The sedimentation rate decreases from core 629, located at the shallowest depth beneath the Nile River plume, to cores 627 and 642. During the interglacials defined by a low 18O/16O ratio, the abundance of tree pollen is maximum and points to an optimum Mediterranean climate with greatest humidity, including some summer rainfall. During glacial maxima, with highest 18O/16O ratio, the pollen abundance is high for steppe and semidesert plants and low for trees, indicating a definitely more arid, more continental, and probably colder climate. The variations of pollen abundance occur in phase with those of the foraminifer δ18O record. This signifies that the regional climate of the Levantine Basin borderlands had the same temporal pattern as the global ice volume documented by the ice volume curve.</style></abstract></record></records></xml>