483 research outputs found
Domain-domain interactions in high mobility group 1 protein (HMG1)
No full textThe high mobility group protein HMG1 is a conserved chromosomal protein with two homologous DNA-binding domains, A and B, and an acidic carboxy-terminal tail, C. The structure of isolated domains A and B has been previously determined by NMR, but the interactions of the different domains within the complete protein were unknown. By means of differential scanning calorimetry and circular dichroism we have investigated the thermal stability of HMG1, of the truncated protein A-B (HMG1 without the acidic tail C) and of the isolated domains A and B. In 3 mM sodium acetate buffer, pH 5, the thermal melting of domains A and B are identical (transition temperature t(m) = 43 degrees C and 41 degrees C, denaturation enthalpies Delta H = 46 kcal.mol(-1)). The thermal melting of protein A-B presents two nearly identical transitions (t(m) = 40 degrees C and 41 degrees C, Delta H = 44 kcal mol(-1) and 46 kcal.mol(-1), respectively). We conclude that the two domains A and B within protein A-B behave as independent domains. The thermal melting of HMG1 is biphasic. The two transitions have a different value of t(m) (38 degrees C and 55 degrees C) and corresponding values of Delta H around 40 kcal.mol(-1). We conclude that within HMG1, the acidic tail C is interacting with one of the two domains A and B, however, the two domains A and B do not interact with each other. At 37 degrees C, one of the two domains A and B, within HMG1, is partly unfolded, whereas the other which interacts with the acidic tail C, is fully native. The interaction free energy of the acidic tail C is estimated to be in the range of 2.5 kcal.mol(-1) based on simulations of the thermograms of HMG1 as a function of the interaction free energy
Supplemental Material for Ramstein and Casler, 2019
No full textFile_S1.csv: Population information
File in .csv format
consisting of information about population assignment and geographical origin
of genotypes
Genotype: population
(in BP) or accesion (in AP) + genotype ID within population/accession: maternal
parent of half-sib families in BP (e.g. ‘Liberty-C2_31804’ refers to genotype
31804 in population Liberty-C2), individual plant in AP (e.g., ‘Dacotah_03’
refers to genotype 03 in accession Dacotah)
Latitude: coordinate
of geographical origin in °N
Longitude: coordinate
of geographical origin in °W
Population: WS4U-C2,
Liberty-C2, U4X-N, U8X-W, U8X-E, U8X-S, L4X-NE or L4X-S
File_S2.csv: Raw phenotypic data
File in .csv format consisting
of trait measurements at plants
Panel: BP (WS4U-C2, Liberty-C2) or AP (U4X-N, U8X-W, U8X-E, U8X-S,
L4X-NE, L4X-S)
Location: WI (for BP) or NY
(for AP)
Year: 2012 to 2014 (for BP),
2009 to 2011 (for AP)
Rep: replicate
Set: set, for AP only (for
which individuals are arranged in a sets-in-reps design)
Genotype: Population (in BP)
or accesion (in AP) + genotype ID within population/accession: maternal parent
of half-sib families in BP, individual plant in AP
PH: plant height,
measured in centimeters as the height from the ground to the top of the tallest
tiller
HD: heading date,
measured in growing degrees days as the cumulated sum of daily average
temperatures (in degrees Celsius; °C) above 10 °C, from January 1st
to the day of heading, defined as the emergence of at least half of the
panicles from the boot; daily average temperatures were estimated by the
average of the minimum and maximum daily temperatures
St: standability,
measured on a 0-10 scale to describe plants’ stature and stiffness, with 0
qualifying plants that are prostrate and 10 qualifying upright and rigid plants
File_S3.csv: Genotype means
File in .csv format
consisting of genotype means for maternal parents in BP and individuals
in AP. In BP, genotype means are the intercept +
two times adjusted half-sib families means. In AP, genotype means are the
intercept + adjusted genotype means. Models used to estimate adjusted half-sib
families means in BP were fitted in WS4U-C2 and Liberty-C2 separately. Models
used to estimate adjusted genotype means in AP were fitted on all AP
individuals.
Genotype: population
(in BP) or accesion (in AP) + genotype ID within population/accession: maternal
parent of half-sib families in BP, individual plant in AP
PH: plant height,
measured in centimeters as the height from the ground to the top of the tallest
tiller
HD: heading date,
measured in growing degrees days as the cumulated sum of daily average
temperatures (in degrees Celsius; °C) above 10 °C, from January 1st
to the day of heading, defined as the emergence of at least half of the
panicles from the boot; daily average temperatures were estimated by the
average of the minimum and maximum daily temperatures
St: standability,
measured on a 0-10 scale to describe plants’ stature and stiffness, with 0
qualifying plants that are prostrate and 10 qualifying upright and rigid plants
Marker_data.rds: Genotype calls
File in .rds format, readable
from the readRDS function in R, containing expected allelic dosages (expected
number of alternate alleles, as per posterior probabilities from genotype
calling) at selected markers for each genotype. Rows correspond to the n = 760 genotypes (maternal parent in
BP, individual in AP). Columns correspond to the m = 717,814 marker loci selected across individuals.
Row names: Population (in BP)
or accesion (in AP) + genotype ID within population/accession: maternal parent
of half-sib families in BP, individual plant in AP
Column name: Chromosome index
+ SNP position as per v1.1 of the reference genome (e.g. ‘Chr05b_1187770’
refers to the SNP at position 1187770 in chromosome 5, subgenome B)</p
Modelling the snowball Earth: from its inception to its aftermath
No full textInternational audienceThe relationship between CO2 variation and Neoproterozoic glaciation has deeply evolved these last years. Through the use of an innovative climate-carbon coupled model, the causes of the CO2 decrease that led to the onset of the global glaciation (Sturtian) has been shown to be strongly related to the dislocation of the Rodinia super continent, promoting CO2 consumption through silicate weathering1. Another important issue is the evolution of atmospheric CO2 during the Snowball episode itself. It appears not to be just a linear accumulation with time through the ongoing solid Earth degassing. Indeed, efficient CO2 diffusion in seawater might have promoted the oceanic crust dissolution, resulting in an asymptotic CO2 rise in the atmosphere2,3, stressing the question of the snowball melting threshold. Indeed, it has been shown that greenhouse climate induced by the storage of the CO2 in the atmosphere invoked to escape a snowball Earth was possibly not sufficient to melt the snowball Earth due to thermal inversion in vertical column4. Therefore, CO2 is may be not the only trigger for the deglaciation. Finally, the super greenhouse climate thought to have followed the snowball episode was explored. We demonstrate that, despite very high temperatures under 0.2 bars of CO2, the amount of rainfall might have been limited by the availability of latent heat which cannot be higher that the total energy provided by the sun. As a consequence of limited increase in the water cycling, CO2 consumption by continental weathering might not exceed 10 times its present day value. The return to normal climatic conditions after the snowball melting should thus have lasted several million of years, further increasing the biological perturbations linked to a snowball event5. The aim of this contribution is to revisit the issue of the role of atmospheric CO2 before, during and after a Snowball Earth and to deliver a new picture of its feedbacks with climate. 1. Donnadieu, Y., Y. Godderis, et al. (2004). "A 'snowball Earth' climate triggered by continental break-up through changes in runoff." Nature 428(6980): 303- 306. 2. Ramstein G., Donnadieu Y., Goddéris Y. Proterozoic glaciations. Comptes Rendus Geoscience 336 (7-8): 639-646 Jun 2004 3. Le Hir G., Goddéris Y., Donnadieu Y., Ramstein G. (2008). A geochemical modelling study of the evolution of the chemical composition of seawater linked to a "snowball" glaciation. Biogeosci. 5, 253-267. 4. Le Hir Guillaume , Goddéris Yves, Donnadieu Yannick , Ramstein Gilles (2008) A scenario for the evolution of the atmopsheric pCO2 during a Snowball Earth, Geology, 36 (1): 47-50 5. Pierrehumbert, R.T. (2004). High levels of atmospheric carbon dioxide necessary for the termination of global glaciation: Nature, v. 429, p. 646-649, doi: 10.1038/nature02640. 6. Le Hir Guillaume, Donnadieu Yannick, Goddéris Y, Pierrehumbert Raymond T., Halverson Galen P., Macouin Mélina, Nédélec Anne b, Ramstein Gilles. (2008).The snowball Earth aftermath: Exploring the limits of continental weathering processes, Earth and Planetary Science Letters, EPSL-09573; No of Pages 11
Modelling the snowball Earth: from its inception to its aftermath
No full textInternational audienceThe relationship between CO2 variation and Neoproterozoic glaciation has deeply evolved these last years. Through the use of an innovative climate-carbon coupled model, the causes of the CO2 decrease that led to the onset of the global glaciation (Sturtian) has been shown to be strongly related to the dislocation of the Rodinia super continent, promoting CO2 consumption through silicate weathering1. Another important issue is the evolution of atmospheric CO2 during the Snowball episode itself. It appears not to be just a linear accumulation with time through the ongoing solid Earth degassing. Indeed, efficient CO2 diffusion in seawater might have promoted the oceanic crust dissolution, resulting in an asymptotic CO2 rise in the atmosphere2,3, stressing the question of the snowball melting threshold. Indeed, it has been shown that greenhouse climate induced by the storage of the CO2 in the atmosphere invoked to escape a snowball Earth was possibly not sufficient to melt the snowball Earth due to thermal inversion in vertical column4. Therefore, CO2 is may be not the only trigger for the deglaciation. Finally, the super greenhouse climate thought to have followed the snowball episode was explored. We demonstrate that, despite very high temperatures under 0.2 bars of CO2, the amount of rainfall might have been limited by the availability of latent heat which cannot be higher that the total energy provided by the sun. As a consequence of limited increase in the water cycling, CO2 consumption by continental weathering might not exceed 10 times its present day value. The return to normal climatic conditions after the snowball melting should thus have lasted several million of years, further increasing the biological perturbations linked to a snowball event5. The aim of this contribution is to revisit the issue of the role of atmospheric CO2 before, during and after a Snowball Earth and to deliver a new picture of its feedbacks with climate. 1. Donnadieu, Y., Y. Godderis, et al. (2004). "A 'snowball Earth' climate triggered by continental break-up through changes in runoff." Nature 428(6980): 303- 306. 2. Ramstein G., Donnadieu Y., Goddéris Y. Proterozoic glaciations. Comptes Rendus Geoscience 336 (7-8): 639-646 Jun 2004 3. Le Hir G., Goddéris Y., Donnadieu Y., Ramstein G. (2008). A geochemical modelling study of the evolution of the chemical composition of seawater linked to a "snowball" glaciation. Biogeosci. 5, 253-267. 4. Le Hir Guillaume , Goddéris Yves, Donnadieu Yannick , Ramstein Gilles (2008) A scenario for the evolution of the atmopsheric pCO2 during a Snowball Earth, Geology, 36 (1): 47-50 5. Pierrehumbert, R.T. (2004). High levels of atmospheric carbon dioxide necessary for the termination of global glaciation: Nature, v. 429, p. 646-649, doi: 10.1038/nature02640. 6. Le Hir Guillaume, Donnadieu Yannick, Goddéris Y, Pierrehumbert Raymond T., Halverson Galen P., Macouin Mélina, Nédélec Anne b, Ramstein Gilles. (2008).The snowball Earth aftermath: Exploring the limits of continental weathering processes, Earth and Planetary Science Letters, EPSL-09573; No of Pages 11
Modelling the snowball Earth: from its inception to its aftermath
No full textInternational audienceThe relationship between CO2 variation and Neoproterozoic glaciation has deeply evolved these last years. Through the use of an innovative climate-carbon coupled model, the causes of the CO2 decrease that led to the onset of the global glaciation (Sturtian) has been shown to be strongly related to the dislocation of the Rodinia super continent, promoting CO2 consumption through silicate weathering1. Another important issue is the evolution of atmospheric CO2 during the Snowball episode itself. It appears not to be just a linear accumulation with time through the ongoing solid Earth degassing. Indeed, efficient CO2 diffusion in seawater might have promoted the oceanic crust dissolution, resulting in an asymptotic CO2 rise in the atmosphere2,3, stressing the question of the snowball melting threshold. Indeed, it has been shown that greenhouse climate induced by the storage of the CO2 in the atmosphere invoked to escape a snowball Earth was possibly not sufficient to melt the snowball Earth due to thermal inversion in vertical column4. Therefore, CO2 is may be not the only trigger for the deglaciation. Finally, the super greenhouse climate thought to have followed the snowball episode was explored. We demonstrate that, despite very high temperatures under 0.2 bars of CO2, the amount of rainfall might have been limited by the availability of latent heat which cannot be higher that the total energy provided by the sun. As a consequence of limited increase in the water cycling, CO2 consumption by continental weathering might not exceed 10 times its present day value. The return to normal climatic conditions after the snowball melting should thus have lasted several million of years, further increasing the biological perturbations linked to a snowball event5. The aim of this contribution is to revisit the issue of the role of atmospheric CO2 before, during and after a Snowball Earth and to deliver a new picture of its feedbacks with climate. 1. Donnadieu, Y., Y. Godderis, et al. (2004). "A 'snowball Earth' climate triggered by continental break-up through changes in runoff." Nature 428(6980): 303- 306. 2. Ramstein G., Donnadieu Y., Goddéris Y. Proterozoic glaciations. Comptes Rendus Geoscience 336 (7-8): 639-646 Jun 2004 3. Le Hir G., Goddéris Y., Donnadieu Y., Ramstein G. (2008). A geochemical modelling study of the evolution of the chemical composition of seawater linked to a "snowball" glaciation. Biogeosci. 5, 253-267. 4. Le Hir Guillaume , Goddéris Yves, Donnadieu Yannick , Ramstein Gilles (2008) A scenario for the evolution of the atmopsheric pCO2 during a Snowball Earth, Geology, 36 (1): 47-50 5. Pierrehumbert, R.T. (2004). High levels of atmospheric carbon dioxide necessary for the termination of global glaciation: Nature, v. 429, p. 646-649, doi: 10.1038/nature02640. 6. Le Hir Guillaume, Donnadieu Yannick, Goddéris Y, Pierrehumbert Raymond T., Halverson Galen P., Macouin Mélina, Nédélec Anne b, Ramstein Gilles. (2008).The snowball Earth aftermath: Exploring the limits of continental weathering processes, Earth and Planetary Science Letters, EPSL-09573; No of Pages 11
Modelling the snowball Earth: from its inception to its aftermath
No full textInternational audienceThe relationship between CO2 variation and Neoproterozoic glaciation has deeply evolved these last years. Through the use of an innovative climate-carbon coupled model, the causes of the CO2 decrease that led to the onset of the global glaciation (Sturtian) has been shown to be strongly related to the dislocation of the Rodinia super continent, promoting CO2 consumption through silicate weathering1. Another important issue is the evolution of atmospheric CO2 during the Snowball episode itself. It appears not to be just a linear accumulation with time through the ongoing solid Earth degassing. Indeed, efficient CO2 diffusion in seawater might have promoted the oceanic crust dissolution, resulting in an asymptotic CO2 rise in the atmosphere2,3, stressing the question of the snowball melting threshold. Indeed, it has been shown that greenhouse climate induced by the storage of the CO2 in the atmosphere invoked to escape a snowball Earth was possibly not sufficient to melt the snowball Earth due to thermal inversion in vertical column4. Therefore, CO2 is may be not the only trigger for the deglaciation. Finally, the super greenhouse climate thought to have followed the snowball episode was explored. We demonstrate that, despite very high temperatures under 0.2 bars of CO2, the amount of rainfall might have been limited by the availability of latent heat which cannot be higher that the total energy provided by the sun. As a consequence of limited increase in the water cycling, CO2 consumption by continental weathering might not exceed 10 times its present day value. The return to normal climatic conditions after the snowball melting should thus have lasted several million of years, further increasing the biological perturbations linked to a snowball event5. The aim of this contribution is to revisit the issue of the role of atmospheric CO2 before, during and after a Snowball Earth and to deliver a new picture of its feedbacks with climate. 1. Donnadieu, Y., Y. Godderis, et al. (2004). "A 'snowball Earth' climate triggered by continental break-up through changes in runoff." Nature 428(6980): 303- 306. 2. Ramstein G., Donnadieu Y., Goddéris Y. Proterozoic glaciations. Comptes Rendus Geoscience 336 (7-8): 639-646 Jun 2004 3. Le Hir G., Goddéris Y., Donnadieu Y., Ramstein G. (2008). A geochemical modelling study of the evolution of the chemical composition of seawater linked to a "snowball" glaciation. Biogeosci. 5, 253-267. 4. Le Hir Guillaume , Goddéris Yves, Donnadieu Yannick , Ramstein Gilles (2008) A scenario for the evolution of the atmopsheric pCO2 during a Snowball Earth, Geology, 36 (1): 47-50 5. Pierrehumbert, R.T. (2004). High levels of atmospheric carbon dioxide necessary for the termination of global glaciation: Nature, v. 429, p. 646-649, doi: 10.1038/nature02640. 6. Le Hir Guillaume, Donnadieu Yannick, Goddéris Y, Pierrehumbert Raymond T., Halverson Galen P., Macouin Mélina, Nédélec Anne b, Ramstein Gilles. (2008).The snowball Earth aftermath: Exploring the limits of continental weathering processes, Earth and Planetary Science Letters, EPSL-09573; No of Pages 11
Base pair opening pathways in B-DNA.
No full textInternational audienceMolecular modeling is used to study the opening pathways of bases within a B-DNA oligomer. It is demonstrated that many open states are possible for a single base pair, although a preference for opening towards the major groove of the double helix is found. In addition we show that opening is strongly influenced by the nature of the base involved and is also coupled in many cases to DNA bending.Molecular modeling is used to study the opening pathways of bases within a B-DNA oligomer. It is demonstrated that many open states are possible for a single base pair, although a preference for opening towards the major groove of the double helix is found. In addition we show that opening is strongly influenced by the nature of the base involved and is also coupled in many cases to DNA bending
1294 Juli 20
No full textHeinrich von Windstein [Kr. Hagenau Els.] beurkundet, daß er an Heinrich von Ramstein und dessen Erben das Dorf rᷝEnwilre mit Gericht und Leuten als rechtmäßiges Lehen verliehen hat. Er hat Heinrich von Ramstein in Besitzrecht und Nutzung des Lehens eingesetzt. -- Bei dem verlehnten Dorf rᷝEnwilre handelt es sich möglicherweise um Engweiler, gelegen 2-3 km nw. Mietesheim, 7-8 km ssw. Niederbronn Begründung: sämtliche in dieser Urk. vorkommenden Ortsbenennungen markieren die Gegend um Niederbronn: Windstein n. Niederbronn, Ramstein = Ruine im Bärenthal b. Philippsburg, nw. Niederbronn, Mvtenſheim = Mietesheim s. Niederbronn, Falkenstein = Ruine nw. Niederbronn, b. Philippsburg. In diesen Umkreis würde sich die vorgeschlagene Lokalisierung »Engweiler⟨ einfügen (Engwiler 1179 urkundl. erwähnt, Schoepflin, Alsatia Diplomatica Bd. I S. 270 Nr. 327). --{'name': 'BAdW', 'uri': 'badw.png'
Thomas Moncure Interview
No full textTwo interviews are available (2005, 2010). COL Moncure commissioned into the United States Air Force in 1972 through the ROTC program at VMI. He graduated from pilot training at Columbus AFB, MS in May 1973 and he served as a command pilot with over 3150 flying hours in B-52, T-38, FB-111A, F-111F, and B-1 aircraft. His other assignments included that of Deputy Director of Plans and Programs, Headquarters United States Air Forces in Europe, Ramstein Air Base, Germany; and Commander and Professor of Aerospace Studies at AFROTC Det 880, Virginia Military Institute. He retired from the Air Force in 2002
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