ライフサイエンスコーパス: phytoplankton

1 d increased tidally induced marine algae and phytoplankton).

2 of carbon, nitrogen and phosphorus found in phytoplankton).

3 isotopic signature similar to that of marine phytoplankton.

4 otosystems for low-light acclimation in many phytoplankton.

5 productivity by decreasing the abundance of phytoplankton.

6 (2) seawater temperature, and (3) biomass of phytoplankton.

7 re among the largest ever recorded in marine phytoplankton.

8 heme b replete and heme b deficient (anemic) phytoplankton.

9 be a key bioavailable source of P for marine phytoplankton.

10 on-specific energy values similar to surface phytoplankton.

11 mulates CO2 consumption by photosynthesizing phytoplankton.

12 Hg concentrations in zooplankton compared to phytoplankton.

13 g cyanobacteria and, potentially, eukaryotic phytoplankton.

14 istributions, but do not correspond to known phytoplankton.

15 ocesses of photosynthesis and respiration in phytoplankton.

16 ve ecosystem impacts down to the smallest of phytoplankton.

17 e the ecological and biogeochemical roles of phytoplankton.

18 Slicks had higher densities of marine phytoplankton (1.7-fold), zooplankton (larval fish prey;

19 Modeled bioaccumulation factors for phytoplankton (10(2.4)-10(5.9)) are more variable than t

20 oncentration that may coincide with peaks in phytoplankton abundance and primary productivity.

21 ffects of the river environmental factors on phytoplankton abundance was temporally inhomogeneous.

22 Phytoplankton account for nearly half of global primary

23 Our analysis reveals seasonal phytoplankton accumulation ('blooming') events occurring

24 oductivity front development with respect to phytoplankton activity (CHL values) and potential predat

25 Freshwater blooms of phytoplankton affect public health and ecosystem service

26 ed the survival of E. affinis over a diet of phytoplankton alone.

27 oniopropionate (DMSP) are produced by marine phytoplankton and bacteria as an important osmolyte to r

28 resent major sources of mortality for marine phytoplankton and bacteria, redirecting the flow of orga

29 g as important chemical links between marine phytoplankton and bacteria.

30 d chlorophyll a, and a shift towards smaller phytoplankton and carnivorous copepods, associated with

31 st and, in part, the third hypotheses: total phytoplankton and cyanobacterial abundance increased in

32 Our hypotheses were that: (a) total phytoplankton and cyanobacterial abundance would be high

33 will lead to a variety of effects on marine phytoplankton and ecosystems.

34 nthic and pelagic energy pathways connecting phytoplankton and fish, (ii) depresses trophic transfer

35 likely consequences for grazing pressures on phytoplankton and hence for biogeochemical cycling, high

36 . oceanica GR in other representative marine phytoplankton and ocean metagenomes.

37 tary statistical analysis of 13 data sets of phytoplankton and periphyton communities exposed to chem

38 tion during evolutionary radiation of marine phytoplankton and provides a model of how new plankton s

39 transformation of anthropogenic chemicals in phytoplankton and suggest that plankton biodiversity cou

40 Furthermore, we found that a mixed diet of phytoplankton and terrestrial material (1:3 carbon ratio

41 Arctic phytoplankton and their response to future conditions sh

42 In closed lakes, interactions involving phytoplankton and their zooplankton grazers play a large

43 At coarse levels of taxonomic aggregation, phytoplankton and zooplankton community composition show

44 plankton evenness explained more variance in phytoplankton and zooplankton resource use efficiency (R

45 were consistently negative and positive for phytoplankton and zooplankton RUE, respectively, and mos

46 Plankton comprises unicellular plants - phytoplankton - and generally small (millimetres or less

47 luid dynamic niches of motile and non-motile phytoplankton, and highlights that rapid responses to hy

48 imals, significant populations of eukaryotic phytoplankton, and the onset of massive phosphorite depo

49 s on respiration and primary productivity of phytoplankton are driven by top-down effects on zooplank

50 Phytoplankton are limited by iron (Fe) in ~40% of the wo

51 rrestrial particulate organic carbon (tPOC), phytoplankton are nutritionally superior and are thought

52 s work supports an improved perspective that phytoplankton are shaped by more nuanced Fe niches in th

53 Phytoplankton are the unicellular photosynthetic microbe

54 an ameliorating impact on the efficiency of phytoplankton as primary mediators of the biological car

55 Cell size influences the rate at which phytoplankton assimilate dissolved inorganic carbon (DIC

56 bly, the oil biodegradation potential of the phytoplankton-associated community exceeded that of the

57 Both nitrogen sources stimulated bulk phytoplankton, bacterial and DOM production and enriched

58 eratures are expected to lead to the loss of phytoplankton biodiversity.

59 ntration in the bay remained at half, as did phytoplankton biomass (C), compared to pretreatment cond

60 rient over-enrichment sufficient to decrease phytoplankton biomass and APPP.

61 orted by stronger correlations found between phytoplankton biomass and LMW-DON than other N forms.

62 s are elements in repeating annual cycles of phytoplankton biomass and they have significant ecologic

63 Temporal changes in phytoplankton biomass are governed by complex predator-p

64 is vertical similarity correlates to surface phytoplankton biomass but not to physical mixing process

65 rthern hemisphere have suggested that annual phytoplankton biomass cycles cannot be fully understood

66 ss processes when modeling future changes in phytoplankton biomass cycles.

67 Ice scour coupled with low phytoplankton biomass drove a phase shift to high mortal

68 While enhanced phytoplankton biomass during the Northeast monsoon is tr

69 ern Ocean to determine key factors governing phytoplankton biomass dynamics over the annual cycle.

70 ant contributors to primary productivity and phytoplankton biomass in coastal and estuarine systems.

71 ependent grazing by microzooplankton reduces phytoplankton biomass near the surface but allows accumu

72 ) to test effects of simulated reductions of phytoplankton biomass or nutrient loadings on trophic cl

73 edenitrification BNR effluents produced more phytoplankton biomass than CAS effluents despite lower N

74 nvestigates a seasonally varying response of phytoplankton biomass to environmental factors in rivers

75 Finally, by varying the amount of phytoplankton biomass we demonstrate that SSA particle p

76 parallel those of chlorophyll-a (an index of phytoplankton biomass).

77 lity (quantified as long-term fluctuation of phytoplankton biomass); rather, the integrated causal pa

78 t (CHL) is commonly described as a proxy for phytoplankton biomass, the size of productivity fronts e

79 mong species richness, nutrient cycling, and phytoplankton biomass, was the best predictor of stabili

80 production was driven primarily by increased phytoplankton biomass, which was likely sustained by an

81 er values for chlorophyll a, 15.8% of summer phytoplankton biovolume and 25.3% of summer zooplankton

82 ) on bacteria-mediated carbon cycling during phytoplankton bloom conditions in the marine environment

83 and atmospheric parameters during the annual phytoplankton bloom cycle.

84 The reason behind the increase in phytoplankton bloom intensity remains unclear, however,

85 pp. abundance, overall copepod abundance and phytoplankton bloom magnitude.

86 movement data with the timing of the spring phytoplankton bloom resulting in increased prey availabi

87 ectrum) over 3 days to represent a transient phytoplankton bloom results in transient subsurface maxi

88 l output (maximum 5 days) to investigate how phytoplankton bloom timing changes in response to projec

89 h one or more environmental factors across a phytoplankton bloom using 16S rRNA gene amplicon communi

90 rred during early summer after a late spring phytoplankton bloom, and were associated with high phosp

91 formula to marine snow formation following a phytoplankton bloom.

92 n (out of nine), coinciding with a declining phytoplankton bloom.

93 to depth through their rapid exploitation of phytoplankton blooms and bulk egestion of rapidly sinkin

94 Phytoplankton blooms are elements in repeating annual cy

95 Recent studies have reported extensive phytoplankton blooms beneath ponded sea ice during summe

96 rm trends in intense summertime near-surface phytoplankton blooms for 71 large lakes globally.

97 Spring phytoplankton blooms in temperate environments contribut

98 y influenced deep waters stimulating massive phytoplankton blooms in the Southern Ocean.

99 es have emerged in the literature to explain phytoplankton blooms, but over time the basic tenets of

100 They frequently form spatially extensive phytoplankton blooms, responding rapidly to increased av

101 despread taxa benefiting from the decline of phytoplankton blooms.

102 acts of global warming on metabolic rates of phytoplankton can be modulated by evolutionary adaptatio

103 , and that marine snow composed of elongated phytoplankton cells can form at high rates also in the a

104 the nutrient-rich region surrounding marine phytoplankton cells, heterotrophic bacterioplankton tran

105 late within the microenvironment surrounding phytoplankton cells, known as the phycosphere.

106 microscale hotspots such as the vicinity of phytoplankton cells.

107 oading (eutrophic vs. hypertrophic) on total phytoplankton chlorophyll-a and cyanobacterial abundance

108 ing the multifaceted biological relevance of phytoplankton chytridiomycosis, resulting from discussio

109 vide a first unambiguous evidence that major phytoplankton classes in Lake Stechlin per se produce CH

110 in 90% acetone to assess the variability in phytoplankton classes, herbivory, and organic matter qua

111 the excretion of interlocking plates by the phytoplankton coccolithophores, can provide a rare windo

112 dinoflagellates successfully persist within phytoplankton communities and even form large blooms dur

113 Such changes can restructure phytoplankton communities and their dynamics, as well as

114 Phytoplankton communities are an essential component of

115 Phytoplankton communities are characterized by an averag

116 Phytoplankton communities are highly diverse functionall

117 his study provides a detailed examination of phytoplankton communities associated with environmental

118 show that individual body masses in tree and phytoplankton communities follow power-law distributions

119 potential effects of high rainfall events on phytoplankton communities is greater loss of biomass thr

120 c understanding of the emergent responses of phytoplankton communities is poor.

121 y manipulated the species richness of marine phytoplankton communities under a range of warming scena

122 Laboratory phytoplankton communities were assembled from pure cultu

123 and rising global temperatures, destabilize phytoplankton communities with major impacts on aquatic

124 control on isotopic fractionation in natural phytoplankton communities.

125 osystems and their importance in structuring phytoplankton communities.

126 yzed a 16-y time series of observations of a phytoplankton community at a nearshore site on the North

127 possessing these pathways in the context of phytoplankton community composition over a 3-week time p

128 ultiple approaches were used to characterize phytoplankton community composition within the Neuse Riv

129 t necessarily in lower AHM rates because the phytoplankton community is able to maintain maximum biom

130 Numerous regional studies have demonstrated phytoplankton community shifts to lightly-silicified dia

131 We suggest a global shift in phytoplankton community structure, for example, a reduct

132 Phytoplankton community structure, which strongly affect

133 ryptophytes were a greater proportion of the phytoplankton community within high nutrient, fresher en

134 By integrating over the whole phytoplankton community, we assigned functional changes

135 ts in global surface ocean light regimes and phytoplankton community-level photoacclimation, these re

136 cteria while preserving algal members of the phytoplankton community.

137 antial amounts of oil that also impacted the phytoplankton community.

138 lity on the metabolome response of a natural phytoplankton community.

139 hanges in population abundance of this major phytoplankton consumer.

140 Eukaryotic phytoplankton critically influence our climate as major

141 All other phytoplankton cultures were sampled in exponential phase

142 hed, the Methods incorrectly stated that all phytoplankton cultures were sampled in mid-exponential p

143 sensitivity of population growth rate across phytoplankton (Cyanobacteria and eukaryotic microalgae)

144 while the population of non-nitrogen-fixing phytoplankton decreases since a larger fraction of fixed

145 etabolic potential in response to a pulse of phytoplankton-derived organic carbon.

146 These same phytoplankton-derived sulfonates support growth requirem

147 ch as exudation and cell lysis release these phytoplankton-derived sulfur metabolites into seawater,

148 ut the interactions between warming, loss of phytoplankton diversity and its impact on the oceans' pr

149 t availability suggests that a 10% change in phytoplankton division rate may be associated with a 50%

150 od from environmental properties controlling phytoplankton division rates (e.g., nutrients and light)

151 simple changes in the seasonal magnitude of phytoplankton division rates.

152 Interactions between bacteria and phytoplankton during bloom events are essential for both

153 ect phytoplankton organisms and regulate the phytoplankton dynamics encompass genes of rhodopsins of

154 nterest in the role of vitamins in governing phytoplankton dynamics, and illuminated amazing versatil

155 e change can significantly influence oceanic phytoplankton dynamics, and thus biogeochemical cycles a

156 e the current understanding of storm-induced phytoplankton dynamics, identify knowledge gaps with a s

157 therefore, might play a major role in global phytoplankton dynamics.

158 d three stages in response to treatments and phytoplankton dynamics.

159 metabolic perturbations induced by AgNPs on phytoplankton, essential organisms in global biogeochemi

160 At the continental scale, phytoplankton evenness explained more variance in phytop

161 For individual regions, slopes of phytoplankton evenness-RUE relationships were consistent

162 Applicability of phytoplankton fluorescence as a quick and effective ecol

163 It is also sensitive to succession in its phytoplankton food, from edible algae in spring to relat

164 Diatoms outcompete other phytoplankton for nitrate, yet little is known about the

165 ate benthic production directly supported by phytoplankton from benthic production recycled through d

166 tates, that within-year ecological change in phytoplankton (from spring diatoms, cryptophytes and gre

167 Diatoms are a diverse and globally important phytoplankton group, responsible for an estimated 20% of

168 the most diverse and ecologically important phytoplankton groups, acting as dominant primary produce

169 tems, infecting representatives of all major phytoplankton groups.

170 The timing of phytoplankton growth (phenology) in tropical oceans is a

171 Marine phytoplankton growth at high latitudes is extensively li

172 rn equatorial Pacific surface waters because phytoplankton growth fueled by nitrate (new production)

173 and concentrated river DOM did not stimulate phytoplankton growth greater than their respective inorg

174 be responsible for stimulating the observed phytoplankton growth in the chicken litter leachate trea

175 ailability of iron (Fe) can seasonally limit phytoplankton growth in the High Latitude North Atlantic

176 ortant nutritional phosphorus (P) source for phytoplankton growth in the ocean, but the contribution

177 ions of metals and nutrients that stimulated phytoplankton growth, resulting in an extensive plume of

178 limiting factors controlling Southern Ocean phytoplankton growth.

179 se the availability of nitrogen often limits phytoplankton growth.

180 entific interest towards fungal parasites of phytoplankton has been gaining momentum in the past few

181 Marine phytoplankton have a crucial role in the modulation of m

182 Here we show that SO phytoplankton have evolved critical adaptations to enhan

183 They repack carbon from inedible phytoplankton hosts into easily ingested chytrid propagu

184 razers even when sterols are absent in their phytoplankton hosts.

185 In phytoplankton, however, the ecophysiological role(s) of

186 ore Emiliania huxleyi is an abundant oceanic phytoplankton, impacting the global cycling of carbon th

187 (Fe) is a growth-limiting micronutrient for phytoplankton in major areas of oceans and deposited win

188 Cyanobacteria are important phytoplankton in the Baltic Sea, an estuarine-like envir

189 d sustain the observed primary production of phytoplankton in the euphotic layer.

190 c cues are important survival strategies for phytoplankton in the ocean.

191 and Synechococcus, the numerically dominant phytoplankton in the oceans, have different responses to

192 trophic linkage between marine bacteria and phytoplankton in the surface ocean is a key step in the

193 ds to reductions in nutrient availability to phytoplankton in the transition zone.

194 or that contributed to the recent decline of phytoplankton in this region and propose a mechanism of

195 ial symbioses exist with autotrophic taxa in phytoplankton, including dinoflagellates, diatoms, and h

196 ses manipulate the physiology and ecology of phytoplankton, influence marine nutrient cycles, and act

197 Marine phytoplankton inhabit a dynamic environment where turbul

198 e of the impact of changes in iron supply on phytoplankton iron status across the Atlantic Ocean.

199 ted by modifying assumptions associated with phytoplankton iron uptake.

200 Monitoring changes in marine phytoplankton is important as they form the foundation o

201 ent and other organisms, yet this process in phytoplankton is poorly defined.

202 Phytoplankton is the base of the marine food chain as we

203 uptake of dissolved methylmercury (MeHg) by phytoplankton is the most important point of entry for M

204 y broadly distributed across major eukaryote phytoplankton lineages and represent three novel classes

205 on sources: biosynthesis by marine bacteria, phytoplankton, macroalgae, and some invertebrate animals

206 s the global nitrogen-fixation rate (because phytoplankton manage with less phosphorus when it is in

207 n sizes and short generation times of marine phytoplankton may allow them to adapt rapidly to global

208 Our study revealed the complexity of phytoplankton metabolism.

209 carbon through the uptake and catabolism of phytoplankton metabolites.

210 sses, which serve to structure infection and phytoplankton mortality in the upper ocean.

211 has been described as a primary mechanism of phytoplankton mortality, little is known about host defe

212 between taxonomic identification methods for phytoplankton, multiple approaches were used to characte

213 e dominance of inedible or poorly nutritious phytoplankton (mycoloop).

214 Considering the phytoplankton nitrogen pool size and dynamics, guanine i

215 In diatoms, a dominant phylum in phytoplankton, NO was reported to mediate programmed cel

216 leocytoplasmic Large DNA Viruses that infect phytoplankton organisms and regulate the phytoplankton d

217 nteraction strengths between zooplankton and phytoplankton over time within and across lakes.

218 We use these results to explain phytoplankton patterns in Massachusetts Bay and to provi

219 Phytoplankton perform half of global biological CO2 upta

220 nkton, perhaps extending survival during low phytoplankton periods, and may help explain elevated zoo

221 Ephemeral "blooms" of picoeukaryotic phytoplankton (PEUK) during spring and after spikes in r

222 of years of data needed to detect a trend in phytoplankton phenology is relatively insensitive to dat

223 Phytoplankton phenology is thus categorised as an 'ecosy

224 the capability of remote sensing to estimate phytoplankton phenology metrics in the northern Red Sea

225 Phytoplankton photosynthesis is often inhibited by ultra

226 lular trait that is important in determining phytoplankton physiological and ecological processes.

227 ng DCM formation has historically focused on phytoplankton physiology (e.g., photoacclimation) and be

228 arine ecosystems, light is a major driver of phytoplankton physiology and ultimately carbon flow thro

229 plankton such as diatoms, and/or a change in phytoplankton physiology during this period, although th

230 Clustering water samples based on phytoplankton pigment composition resulted in robust but

231 Phytoplankton play key roles in the oceans by regulating

232 By this definition, we observed anemic phytoplankton populations in the Subtropical South Atlan

233 both abiotic (ocean temperature) and biotic (phytoplankton prey) drivers.

234 om benthic and aeolian sources, iron reaches phytoplankton primarily when iron-rich subsurface waters

235 ication of marine ecosystems based on annual phytoplankton primary production (APPP), with categories

236 s in the Arctic Ocean has promoted increased phytoplankton primary production because of the greater

237 Phytoplankton primary production is at the base of the m

238 However, estuarine phytoplankton primary productivity abundances can wax an

239 Fossil-fuel emissions may impact phytoplankton primary productivity and carbon cycling by

240 We analysed the time series of phytoplankton primary productivity at BATS site using ma

241 stuary (SFE), an estuary with relatively low phytoplankton primary productivity.

242 tes) exists among key lineages of eukaryotic phytoplankton producers and heterotrophic bacterial cons

243 opportunity to explore effects of warming on phytoplankton production across the vast oligotrophic oc

244 Global warming is thought to affect phytoplankton production both directly, by impacting the

245 The former will track the dynamics of phytoplankton production more closely than the latter.

246 this shift in N-loading influences estuarine phytoplankton production, nutrient addition bioassays we

247 upper ocean, induced a negative feedback on phytoplankton productivity by reducing the availability

248 Phytoplankton productivity in the polar Southern Ocean (

249 physical forcing, ice retreat patterns, and phytoplankton productivity.

250 in seawater, which can readily be reduced by phytoplankton, provides a freely available source of sul

251 0.67 and 0.96), indicating a strong link to phytoplankton-related processes.

252 Primary production by phytoplankton represents a major pathway whereby atmosph

253 inance are unclear, we experimentally tested phytoplankton responses to a gradient of N loading in a

254 than photosynthesis across 18 diverse marine phytoplankton, resulting in universal declines in the ra

255 ophyll-a (Chl-a) is used to track changes in phytoplankton, since there are global, regular satellite

256 t organic sulfur metabolite produced by many phytoplankton species and degraded by bacteria via two d

257 The identification of phytoplankton species and microbial biodiversity is nece

258 Since many phytoplankton species are elongated, these results sugge

259 a bloom is too high, or when toxin-producing phytoplankton species are present.

260 ltures of Prochlorococcus, the most abundant phytoplankton species in the global ocean, were used as

261 Here, we investigated how phytoplankton species richness (SR) and class richness (

262 CCM) to quantify the causal networks linking phytoplankton species richness, biomass, and physicochem

263 a potential recognition cascade in a marine phytoplankton species that parallels better-understood v

264 e rates, as proxies of metabolic rates, of 3 phytoplankton species using nanoscale secondary ion mass

265 erally results in unselective elimination of phytoplankton species, disrupting water ecology and envi

266 uptake systems to influence the fitness of a phytoplankton species.

267 The timing of the annual phytoplankton spring bloom is likely to be altered in re

268 ce cover and duration predetermine levels of phytoplankton stock and thus, influence virioplankton by

269 ure, for example, a reduction in (13) C-rich phytoplankton such as diatoms, and/or a change in phytop

270 Unicellular eukaryotic phytoplankton, such as diatoms, rely on microbial commun

271 proof-of-concept experiments with freshwater phytoplankton supporting such framework.

272 nce in biogeochemical cycles, cyanobacterium-phytoplankton symbioses remain understudied and poorly u

273 o chytrids infecting two major bloom-forming phytoplankton taxa of contrasting nutritional value: the

274 We find that cultured eukaryotic phytoplankton taxa produce sulfonates, often at millimol

275 cific groups of bacterial DMSP degraders and phytoplankton taxa.

276 onferring an ecological advantage over other phytoplankton taxa.

277 Crocosphaera exists with non-nitrogen-fixing phytoplankton, the relative abundance of Crocosphaera in

278 rious effects of strong turbulence on motile phytoplankton, these results point to an active adaptati

279 Marine phytoplankton thus possess unique signaling mechanisms t

280 Using mesocosms we exposed phytoplankton to ambient (390 muatm) or future CO(2) lev

281 he universality of plant self-thinning, from phytoplankton to complex canopies, likely the consequenc

282 The strategies used by these phytoplankton to extract iron from seawater constrain ca

283 ury, across a range of taxonomic groups from phytoplankton to fish and marine mammals.

284 ncludes numerous trophic levels ranging from phytoplankton to polar bears.

285 ed organic phosphorus (DOP) is important for phytoplankton to survive the scarcity of dissolved inorg

286 affecting open-ocean marine ecosystems from phytoplankton to top predators.

287 The capacity of phytoplankton to utilize dissolved organic phosphorus (D

288 In the surface ocean, phytoplankton transform inorganic substrates into organi

289 Laboratory incubations of different phytoplankton types and application of stable isotope te

290 hange, large-scale atmospheric dynamics, and phytoplankton variability.

291 the genetic diversity of several eukaryotic phytoplankton virus groups has been characterized, their

292 We identify in the genome of a phytoplankton virus, which infects the small green alga

293 ar population models of interactions between phytoplankton, viruses and grazers as a means to quantit

294 mics, and illuminated amazing versatility in phytoplankton vitamin metabolism.

295 ice conditions and isotopic fractionation by phytoplankton, we explain the decadal decline in delta(1

296 ed by Schoenoplectus sp., or tule) even when phytoplankton were abundant and tPOC was scarce.

297 mbinations of known exometabolites of marine phytoplankton were inoculated with seawater bacterial as

298 fluence the growth of dinitrogen (N2)-fixing phytoplankton, which contribute a large fraction of prim

299 o ammonia, which can be used by microbes and phytoplankton, while denitrification/anammox effectively

300 intensify in the future, the assumption that phytoplankton will readily adapt to rising temperatures