Regulation of p53 antiproliferative function by transactivation domain phosphorylation at threonine 18 and serine 20

We investigated the induction and physiological role of Thr18 and Ser20 phosphorylation of p53 in response to DNA damage caused by treatment with ionizing (IR) or ultraviolet (UV) radiation. Polyclonal antibodies specifically recognizing phospho-Thr18 and phospho-Ser20 were used to detect p53 phosphorylation in vivo. Analyses of five wild-type (wt) p53 containing cell lines revealed lineage specific differences in phosphorylation of Thr18 and Ser20 after treatment with IR or UV. Importantly, the phosphorylation of p53 at Thr18 and Ser20 correlated with induction of the p53 downstream targets p21Waf1/Cip1 (p21) and Mdm-2, suggesting a transactivation enhancing role for Thr18 and Ser20 phosphorylation. Whereas Thr18 phosphorylation appears to abolish side-chain hydrogen bonding between Thr18 and Asp21, Ser20 phosphorylation may introduce charge attraction between Ser20 and Lys24. Both of these interactions could contribute to stabilizing α-helical conformation within the p53 transactivation domain. Mutagenesis-derived phosphorylation mimicry of p53 at Thr18 and Ser20 by Asp substitution (p53T18D/S20D) altered transactivation domain conformation and significantly reduced the interaction of p53 with the transactivation repressor Mdm-2. Mdm-2 interaction was also reduced with p53 containing a single site Asp substitution at Ser20 (p53S20D) and with the Thr18/Asp21 hydrogen bond disrupting p53 mutants p53T18A, p53T18D and p53D21A. In contrast, no direct effect was observed on the interaction of p53T18A, p53T18D and p53D21A with the basal transcription factor TAF II31. However, prior incubation of p53T18A, p53T18D and p53D21A with Mdm-2 modulated TAFII31 interaction, suggesting Mdm-2 blocks the accessibility of p53 to TAFII31. Consistently, p53-null cells transfected with p53S20D and p53T18A, p53T18D and p53D21A demonstrated enhanced endogenous p21 expression; transfection with p53T18D/S20D most significantly enhanced p21 and fas/APO-1 (fas ) expression. Expression of p53T18A, p53T18D and p53D21A in p53/Mdm-2-double null cells exhibited no discernible differences in p21 expression. Cell proliferation was also significantly curtailed in p53-null cells transfected with p53T18D/S20D relative to cells transfected with wt p53. We conclude the irradiation-induced phosphorylation of p53 at Thr18 and Ser20 alters the α-helical conformation of its transactivation domain. Altered conformation reduces direct interaction with the transrepressor Mdm-2, enhancing indirect recruitment of the basal transcription factor TAFII31, facilitating sequence-specific transactivation function resulting in proliferative arrest. ^

Isotopic signature of specific biomarkers derived from anaerobic methanotrophic archaea (ANME groups) and sulphate-reducing bacteria (SRB) at different cold seep provinces

Anaerobic methane-oxidizing microbial communities in sediments at cold methane seeps are important factors in controlling methane emission to the ocean and atmosphere. Here, we investigated the distribution and carbon isotopic signature of specific biomarkers derived from anaerobic methanotrophic archaea (ANME groups) and sulphate-reducing bacteria (SRB) responsible for the anaerobic oxidation of methane (AOM) at different cold seep provinces of Hydrate Ridge, Cascadia margin. The special focus was on their relation to in situ cell abundances and methane turnover. In general, maxima in biomarker abundances and minima in carbon isotope signatures correlated with maxima in AOM and sulphate reduction as well as with consortium biomass. We found ANME-2a/DSS aggregates associated with high abundances of sn-2,3-di-O-isoprenoidal glycerol ethers (archaeol, sn-2-hydroxyarchaeol) and specific bacterial fatty acids (C16:1omega5c, cyC17:0omega5,6) as well as with high methane fluxes (Beggiatoa site). The low to medium flux site (Calyptogena field) was dominated by ANME-2c/DSS aggregates and contained less of both compound classes but more of AOM-related glycerol dialkyl glycerol tetraethers (GDGTs). ANME-1 archaea dominated deeper sediment horizons at the Calyptogena field where sn-1,2-di-O-alkyl glycerol ethers (DAGEs), archaeol, methyl-branched fatty acids (ai-C15:0, i-C16:0, ai-C17:0), and diagnostic GDGTs were prevailing. AOM-specific bacterial and archaeal biomarkers in these sediment strata generally revealed very similar d13C-values of around -100 per mill. In ANME-2-dominated sediment sections, archaeal biomarkers were even more 13C-depleted (down to -120 per mill), whereas bacterial biomarkers were found to be likewise 13C-depleted as in ANME-1-dominated sediment layers (d13C: -100 per mill). The zero flux site (Acharax field), containing only a few numbers of ANME-2/DSS aggregates, however, provided no specific biomarker pattern. Deeper sediment sections (below 20 cm sediment depth) from Beggiatoa covered areas which included solid layers of methane gas hydrates contained ANME-2/DSS typical biomarkers showing subsurface peaks combined with negative shifts in carbon isotopic compositions. The maxima were detected just above the hydrate layers, indicating that methane stored in the hydrates may be available for the microbial community. The observed variations in biomarker abundances and 13C-depletions are indicative of multiple environmental and physiological factors selecting for different AOM consortia (ANME-2a/DSS, ANME-2c/DSS, ANME-1) along horizontal and vertical gradients of cold seep settings.

Phytol and phytyldiol concentrations at DYFAMED time series station and sediment trap

Particulate samples from the water column were collected monthly from depths of 5-150 m, between May 1996 and March 1997, in the northwestern Mediterranean Sea (Ligurian Sea) as part of the DYFAMED project within the French JGOFS program. These samples were analyzed by gas chromatography-electron impact mass spectrometry for their phytol and 3-methylidene-3,7,11-trimethylhexadecan-1,2-diol (phytyldiol) content. The corresponding Chlorophyll Phytyl side chain Photodegradation Index, molar ratio of phytyldiol to phytol, was calculated and the mean amount of chlorophyll photodegraded within the euphotic zone estimated. Seasonal differences in the chlorophyll photodegradation process appear in the one-year study. The chlorophyll appeared more photodegraded in the surface water (generally more than 40% photodegraded at 5-10 m) than at the deep chlorophyll maximum (DCM) (40-50 m) observed in the summer stratified waters (about 20% photodegraded). This difference was attributed to the healthy state of the phytoplankton community (coincidence with the highest primary production levels) and to the lower intensity of irradiance at the DCM level. On the other hand, the bulk of the detrital chlorophyll (chlorophyll associated with phytodetritus, phaeopigments) undergoes photodegradation before it sinks out of the photic zone. However, in January (winter mixed water) the pigments exported towards the sea floor were less photodegraded. This is thought to result from a shorter period of residence of the pigments in the photic zone due to vertical convection and grazing activity of macrozooplankton (salps), which are producers of rapid sinking fecal pellets.

Geochemistry of ODP Sites 123-765 and 123-766

The sediments of the Argo and Gascoyne abyssal plains are generally lean in organic matter, are immature, and contain hydrocarbons trapped during sediment deposition rather than those generated during sediment catagenesis. TOC concentrations in the Argo Abyssal Plain Cenozoic sediments are 0.5 wt%, and organic matter appears to be from mixed marine and reworked, degraded, organic matter sources, with the latter being contributed by turbidity flows from the nearby continental margin. TOC concentrations within the Cenozoic sediments of the Gascoyne Abyssal Plain are mostly undetectable (<0.1 wt%). Biomarker distributions determined by gas chromatography (GC) and gas chromatography-mass spectrometry (GCMS) indicate that organic matter extracted from the Lower Cretaceous sediments from both sites is predominantly marine with varying contributions from terrestrial organic matter. The specific marine biomarker, 24-n-propylcholestane is in relatively high abundance in all samples. In addition, the relatively high abundance of the 4-methylsteranes with the 23,24-dimethyl side chain (in all samples) indicates significant dinoflagellate contributions and marine organic matter. The ratios of n-C27/n-C17 reflect relative contributions of marine vs. terrestrial organic matter. TOC, while generally low at Argo, is relatively high near the Barremian/Aptian boundary (one sample has a TOC of 5.1 wt%) and the Aptian/Albian boundary (up to 1.3 wt% TOC), and two samples from the Barremian and Aptian sections contain relatively high proportions of terrestrial organic carbon. TOC values in the Lower Cretaceous sediments from Gascoyne Abyssal Plain are low (<0.1 wt%) near the Aptian/Barremian boundary. TOC values are higher in older sediments, with maxima in the upper Barremian (1.02 wt%), the Barremian/Hauterivian (0.6 wt%), and Valanginian (1.8 wt%). Sediments from the upper Barremian contain higher amounts of terrestrial organic carbon than older sediments.