Climate-Driven Basin-Scale Decadal Oscillations of Oceanic Phytoplankton

Martínez, Élodie; Antoine, David; D’Ortenzio, Fabrizio; Gentili, Bernard

doi:10.1126/science.1177012

Cited by 262 publications

(212 citation statements)

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“…Cod recruitment covaries positively with phytoplankton and zooplank- ton (C. finmarchicus and Calanus helgolandicus) abundance due to reduced food (zooplankton availability and quality) (26). Since 1958 increasing temperatures have reduced the quality of zooplanktonic food available for larval/juvenile cod [progressive substitution of C. finmarchicus by C. helgolandicus at higher temperatures (25)], mediated by changes in water column stratification (49,50), leading to poor recruitment to adult populations in the North Sea (26). In addition, decline in food availability has exacerbated the decline of European cod stocks due to overfishing (7).…”

Section: Resultsmentioning

confidence: 99%

North Atlantic summers have warmed more than winters since 1353, and the response of marine zooplankton

Kamenos

2010

Proc. Natl. Acad. Sci. U.S.A.

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Modeling and measurements show that Atlantic marine temperatures are rising; however, the low temporal resolution of models and restricted spatial resolution of measurements (i) mask regional details critical for determining the rate and extent of climate variability, and (ii) prevent robust determination of climatic impacts on marine ecosystems. To address both issues for the North East Atlantic, a fortnightly resolution marine climate record from 1353-2006 was constructed for shallow inshore waters and compared to changes in marine zooplankton abundance. For the first time summer marine temperatures are shown to have increased nearly twice as much as winter temperatures since 1353. Additional climatic instability began in 1700 characterized by ∼5-65 year climate oscillations that appear to be a recent phenomenon. Enhanced summer-specific warming reduced the abundance of the copepod Calanus finmarchicus, a key food item of cod, and led to significantly lower projected abundances by 2040 than at present. The faster increase of summer marine temperatures has implications for climate projections and affects abundance, and thus biomass, near the base of the marine food web with potentially significant feedback effects for marine food security.coralline algae | rhodolith | maerl | seasonal P rior to instrumentally derived temperature records that began in the 1850s, knowledge of seasonal and regional-scale marine temperature changes at high latitudes is limited. Thus at present, hemispheric Atlantic climatic patterns are deduced from multiproxy and instrumental networks using statistical (1, 2) and modeling (3) approaches. Whereas such approaches show that the Atlantic Multidecadal Oscillation (AMO), the North Atlantic Oscillation (NAO), and Atlantic Meridional Overturning Circulation (AMOC) have a substantial influence on Atlantic climate (e.g., ref. 4) they are still unable to capture details that are critical for determining the spatiotemporal distribution of climate oscillations (5, 6) and their associated impacts (7). For example, whereas the AMO, which models suggest reflects multidecadal variation in the AMOC (8), is the dominant influence on summer climate in the United Kingdom (9), at higher European latitudes, seasonal terrestrial tree-ring climate records (6, 10) are not representative of high-latitude sea surface temperatures (11). Limited spatiotemporal resolution, absent proxy validation and organism effects have restricted the distribution of current inshore proxy-derived sea surface temperature (SST) records (12-16). Therefore to date, we have a poor understanding of season specific temperature variability. Similarly, SST, AMO, and AMOC variations are not well represented at high spatiotemporal resolution beyond the instrumental record in North East Atlantic shallow inshore waters (for example 55°50'N 05°50'W). This information is needed to better understand rates of regional climate variability (5).Marine responses to such climate fluctuations are reflected in the productivity of marine ecosystems f...

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Section: Resultsmentioning

confidence: 99%

North Atlantic summers have warmed more than winters since 1353, and the response of marine zooplankton

Kamenos

2010

Proc. Natl. Acad. Sci. U.S.A.

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“…Climate variables are assessed, where this is helpful for interpreting the carbon simulation. For example, the land carbon balance is mainly controlled by surface temperature and precipitation (Piao et al, 2009), whereas the ocean carbon balance is mainly influenced by sea surface temperature (SST) and mixed layer depth (MLD) (Martinez et al, 2009).…”

Section: Observationsmentioning

confidence: 99%

The carbon cycle in the Australian Community Climate and Earth System Simulator (ACCESS-ESM1) – Part 2: Historical simulations

et al. 2017

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Abstract. Over the last decade many climate models have evolved into Earth system models (ESMs), which are able to simulate both physical and biogeochemical processes through the inclusion of additional components such as the carbon cycle. The Australian Community Climate and Earth System Simulator (ACCESS) has been recently extended to include land and ocean carbon cycle components in its ACCESS-ESM1 version. A detailed description of ACCESS-ESM1 components including results from pre-industrial simulations is provided in Part 1. Here, we focus on the evaluation of ACCESS-ESM1 over the historical period in terms of its capability to reproduce climate and carbon-related variables. Comparisons are performed with observations, if available, but also with other ESMs to highlight common weaknesses. We find that climate variables controlling the exchange of carbon are well reproduced. However, the aerosol forcing in ACCESS-ESM1 is somewhat larger than in other models, which leads to an overly strong cooling response in the land from about 1960 onwards. The land carbon cycle is evaluated for two scenarios: running with a prescribed leaf area index (LAI) and running with a prognostic LAI. We overestimate the seasonal mean (1.7 vs. 1.4) and peak amplitude (2.0 vs. 1.8) of the prognostic LAI at the global scale, which is common amongst CMIP5 ESMs. However, the prognostic LAI is our preferred choice, because it allows for the vegetation feedback through the coupling between LAI and the leaf carbon pool. Our globally integrated land-atmosphere flux over the historical period is 98 PgC for prescribed LAI and 137 PgC for prognostic LAI, which is in line with estimates of land use emissions (ACCESS-ESM1 does not include land use change).The integrated ocean-atmosphere flux is 83 PgC, which is in agreement with a recent estimate of 82 PgC from the Global Carbon Project for the period 1959-2005. The seasonal cycle of simulated atmospheric CO 2 is close to the observed seasonal cycle (up to 1 ppm difference for the station at Mace Head and up to 2 ppm for the station at Mauna Loa), but shows a larger amplitude (up to 6 ppm) in the high northern latitudes. Overall, ACCESS-ESM1 performs well over the historical period, making it a useful tool to explore the change in land and oceanic carbon uptake in the future.

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“…These two techniques may be used to partition TCHLa into three phytoplankton size classes (PSC), micro-(N20 μm), nano-(2-20 μm) and pico-phytoplankton (b2 μm). Recent studies illustrate a tight coupling between TCHLa, PSC and physical forcing (Behrenfeld et al, 2006;Martinez et al, 2009;Kostadinov et al, 2010;Brewin et al, 2012). However, long-term changes in these two ecological indicators remain non-trivial to evaluate (e.g.…”

Section: Introductionmentioning

confidence: 99%

Temporal changes in total and size-fractioned chlorophyll-a in surface waters of three provinces in the Atlantic Ocean (September to November) between 2003 and 2010

Ağırbaş

Martinez‐Vicente

Brewin

et al. 2015

Journal of Marine Systems

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Phytoplankton total chlorophyll concentration (TCHLa) and phytoplankton size structure are two important ecological indicators in biological oceanography. Using high performance liquid chromatography (HPLC) pigment data, collected from surface waters along the Atlantic Meridional Transect (AMT), we examine temporal changes in TCHLa and phytoplankton size class (PSC: micro-, nano-and pico-phytoplankton) between 2003 and 2010 (September to November cruises only), in three ecological provinces of the Atlantic Ocean. The HPLC data indicate no significant change in TCHLa in northern and equatorial provinces, and an increase in the southern province. These changes were not significantly different to changes in TCHLa derived using satellite oceancolour data over the same study period. Despite no change in AMT TCHLa in northern and equatorial provinces, significant differences in PSC were observed, related to changes in key diagnostic pigments (fucoxanthin, peridinin, 19′-hexanoyloxyfucoxanthin and zeaxanthin), with an increase in small cells (nano-and picophytoplankton) and a decrease in larger cells (micro-phytoplankton). When fitting a three-component model of phytoplankton size structure -designed to quantify the relationship between PSC and TCHLa to each AMT cruise, model parameters varied over the study period. Changes in the relationship between PSC and TCHLa have wide implications in ecology and marine biogeochemistry, and provide key information for the development and use of empirical ocean-colour algorithms. Results illustrate the importance of maintaining a timeseries of in-situ observations in remote regions of the ocean, such as that acquired in the AMT programme.

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Climate-Driven Basin-Scale Decadal Oscillations of Oceanic Phytoplankton

Cited by 262 publications

References 24 publications

North Atlantic summers have warmed more than winters since 1353, and the response of marine zooplankton

North Atlantic summers have warmed more than winters since 1353, and the response of marine zooplankton

The carbon cycle in the Australian Community Climate and Earth System Simulator (ACCESS-ESM1) – Part 2: Historical simulations

Temporal changes in total and size-fractioned chlorophyll-a in surface waters of three provinces in the Atlantic Ocean (September to November) between 2003 and 2010

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