TY - JOUR
T1 - A 1.8 million year history of Amazon vegetation
AU - Kern, Andrea K.
AU - Akabane, Thomas Kenji
AU - Ferreira, Jaqueline Q.
AU - Chiessi, Cristiano M.
AU - Willard, Debra A.
AU - Ferreira, Fabricio
AU - Sanders, Allan Oliveira
AU - Silva, Cleverson G.
AU - Rigsby, Catherine
AU - Cruz, Francisco W.
AU - Dwyer, Gary S.
AU - Fritz, Sherilyn C.
AU - Baker, Paul A.
N1 - Funding Information:
Poaceae is the most abundant pollen taxon found in CDH-79, which showed a significant, somewhat step-wise, decrease from the base towards the top of the core (Fig. 3E; 4). Average values of 60% in older samples decreased after 1300 ka to levels around 50%. These values persisted until approximately 700 ka, when the abundance again decreased to about 40% in the entire remaining portion of the record. PCA (supplementary material) supports a major shift in the pollen assemblages between 900 and 700 ka considering all samples and all pollen taxa.Funding was provided by grants from FAPESP 2014/05582–0, 2012/50260–6, 2015/18314–7 to A.K.K.; and from NSF (EAR-1812681 and OCE-0823650) to P.A.B.; and NSF (EAR-1812857) to S.C.F. This research was partially funded through the 2019–2020 BiodivERsA joint call for research proposals, under the BiodivClim ERA-Net COFUND program, and with the funding organization FAPESP (grant 2019/24349–9). C.M.C. acknowledges the financial support from FAPESP (grant 2018/15123–4) and CNPq (grant 312458/2020–7). F.F. has the support of the Brazilian agency CAPES [grant numbers 88882.151083/2017–01, and 88881.185132/2018–01. T.K.A. acknowledges the financial support from FAPESP (grant 2019/19948–0). D.W. was supported by the U.S. Geological Survey Land Change Science/Climate Research & Development Program. Any use of trade, firm, or product names is for descriptive purposes only and does not imply endorsement by the U.S. Government We thank the officers, crew, and support personnel of the R/V Knorr and WHOI. We especially acknowledge the long-core coring team. The innovative design work, tireless deck work, and leadership of James Broda were indispensable. The work was made possible by the cooperation of the Brazilian navy and the government of Brazil. We acknowledge Frank Mayle (University of Reading) for access to his pollen collection.
Funding Information:
Funding was provided by grants from FAPESP 2014/05582–0, 2012/50260–6, 2015/18314–7 to A.K.K.; and from NSF (EAR-1812681 and OCE-0823650) to P.A.B.; and NSF (EAR-1812857) to S.C.F.. This research was partially funded through the 2019–2020 BiodivERsA joint call for research proposals, under the BiodivClim ERA-Net COFUND program, and with the funding organization FAPESP (grant 2019/24349–9). C.M.C. acknowledges the financial support from FAPESP (grant 2018/15123–4) and CNPq (grant 312458/2020–7). F.F. has the support of the Brazilian agency CAPES [grant numbers 88882.151083/2017–01, and 88881.185132/2018–01. T.K.A. acknowledges the financial support from FAPESP (grant 2019/19948–0). D.W. was supported by the U.S. Geological Survey Land Change Science/Climate Research & Development Program. Any use of trade, firm, or product names is for descriptive purposes only and does not imply endorsement by the U.S. Government We thank the officers, crew, and support personnel of the R/V Knorr and WHOI. We especially acknowledge the long-core coring team. The innovative design work, tireless deck work, and leadership of James Broda were indispensable. The work was made possible by the cooperation of the Brazilian navy and the government of Brazil. We acknowledge Frank Mayle (University of Reading) for access to his pollen collection.
Publisher Copyright:
© 2022 Elsevier Ltd
PY - 2023/1/1
Y1 - 2023/1/1
N2 - During the Pleistocene, long-term trends in global climate were controlled by orbital cycles leading to high amplitude glacial-interglacial variability. The history of Amazonian vegetation during this period is largely unknown since no continuous record from the lowland basin extends significantly beyond the last glacial stage. Here we present a paleoenvironmental record spanning the last 1800 kyr based on palynological data, biome reconstructions, and biodiversity metrics from a marine sediment core that preserves a continuous archive of sediments from the Amazon River. Tropical rainforests dominated the Amazonian lowlands during the last 1800 ka interchanging with surrounding warm-temperate rainforests and tropical seasonal forests. Between 1800 and 1000 ka, rainforest biomes were present in the Amazon drainage basin, along with extensive riparian wetland vegetation. Tropical rainforest expansion occurred during the relatively warm Marine Isotope Stages 33 and 31 (ca. 1110 to 1060 ka), followed by a contraction of both forests and wetlands until ca. 800 ka. Between 800 and 400 ka, low pollen concentration and low diversity of palynological assemblages renders difficult the interpretation of Amazonian vegetation. A strong synchronicity between vegetation changes and glacial-interglacial global climate cycles was established around 400 ka. After 400 ka, interglacial vegetation was dominated by lowland tropical rainforest in association with warmer temperatures and higher CO2. During cooler temperatures and lower CO2 of glacial stages, tropical seasonal forests expanded, presumably towards eastern Amazonia. While this study provides no evidence supporting a significant expansion of savanna or steppe vegetation within the Amazonian lowlands during glacial periods, there were changes in the rainforest composition in some parts of the basin towards a higher proportion of deciduous elements, pointing to less humid conditions and/or greater seasonality of precipitation. Nevertheless, rainforest persisted during both glacial and interglacial periods. These findings confirm the sensitivity of tropical lowland vegetation to changes in CO2, temperature, and moisture availability and the most suitable conditions for tropical rainforests occurred during the warmest stages of the Mid Pleistocene Transition and during the interglacial stages of the past 400 kyr.
AB - During the Pleistocene, long-term trends in global climate were controlled by orbital cycles leading to high amplitude glacial-interglacial variability. The history of Amazonian vegetation during this period is largely unknown since no continuous record from the lowland basin extends significantly beyond the last glacial stage. Here we present a paleoenvironmental record spanning the last 1800 kyr based on palynological data, biome reconstructions, and biodiversity metrics from a marine sediment core that preserves a continuous archive of sediments from the Amazon River. Tropical rainforests dominated the Amazonian lowlands during the last 1800 ka interchanging with surrounding warm-temperate rainforests and tropical seasonal forests. Between 1800 and 1000 ka, rainforest biomes were present in the Amazon drainage basin, along with extensive riparian wetland vegetation. Tropical rainforest expansion occurred during the relatively warm Marine Isotope Stages 33 and 31 (ca. 1110 to 1060 ka), followed by a contraction of both forests and wetlands until ca. 800 ka. Between 800 and 400 ka, low pollen concentration and low diversity of palynological assemblages renders difficult the interpretation of Amazonian vegetation. A strong synchronicity between vegetation changes and glacial-interglacial global climate cycles was established around 400 ka. After 400 ka, interglacial vegetation was dominated by lowland tropical rainforest in association with warmer temperatures and higher CO2. During cooler temperatures and lower CO2 of glacial stages, tropical seasonal forests expanded, presumably towards eastern Amazonia. While this study provides no evidence supporting a significant expansion of savanna or steppe vegetation within the Amazonian lowlands during glacial periods, there were changes in the rainforest composition in some parts of the basin towards a higher proportion of deciduous elements, pointing to less humid conditions and/or greater seasonality of precipitation. Nevertheless, rainforest persisted during both glacial and interglacial periods. These findings confirm the sensitivity of tropical lowland vegetation to changes in CO2, temperature, and moisture availability and the most suitable conditions for tropical rainforests occurred during the warmest stages of the Mid Pleistocene Transition and during the interglacial stages of the past 400 kyr.
KW - Biodiversity
KW - Glacial-interglacial cycles
KW - Mid-pleistocene transition
KW - Palynology
KW - South America
KW - Vegetation
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U2 - 10.1016/j.quascirev.2022.107867
DO - 10.1016/j.quascirev.2022.107867
M3 - Article
AN - SCOPUS:85142675427
SN - 0277-3791
VL - 299
JO - Quaternary Science Reviews
JF - Quaternary Science Reviews
M1 - 107867
ER -