Serum folate, cobalamin, homocysteine and methylmalonic acid concentrations in pigs with acute, chronic or subclinical Lawsonia intracellularis infection.

Lawsonia intracellularis is the causative agent of porcine proliferative enteropathy. The clinical presentation can be acute (i.e. proliferative hemorrhagic enteropathy, PHE), chronic (i.e. porcine intestinal adenomatosis, PIA) or subclinical. In humans with chronic enteropathies, low serum folate (vitamin B(9)) and cobalamin (vitamin B(12)) concentrations have been associated with increased serum concentrations of homocysteine and methylmalonic acid (MMA), which reflect the availability of both vitamins at the cellular level. The aim of this study was to evaluate serum folate, cobalamin, homocysteine and MMA concentrations in serum samples from pigs with PHE, PIA or subclinical L. intracellularis infection, and in negative controls. Serum folate, cobalamin, homocysteine and MMA concentrations differed significantly among pigs in the PHE, PIA, subclinical and negative control groups. Serum folate concentrations in the PHE and PIA groups were lower than in the subclinical and negative control groups, while serum cobalamin concentrations were lower in the PIA group than in other groups. Serum concentrations of homocysteine were higher in the PHE, PIA and subclinical groups than in the negative control group. Serum concentrations of MMA were higher in the subclinical and PIA groups than in the control group. These data suggest that pigs infected with L. intracellularis have altered serum cobalamin, folate, homocysteine and MMA concentrations.

The triplite–triploidite supergroup: structural modulation in wagnerite, discreditation of magniotriplite, and the new mineral hydroxylwagnerite

Electron-microprobe analysis, single-crystal X-ray diffraction with an area detector, and high-resolution transmission electron microscopy show that minerals related to wagnerite, triplite and triploidite, which are monoclinic Mg, Fe and Mn phosphates with the formula Me2+ 2PO4(F,OH), constitute a modulated series based on the average triplite structure. Modulation occurs along b and may be commensurate with (2b periodicity) or incommensurate but generally close to integer values (∼3b, ∼5b, ∼7b, ∼9b), i.e. close to polytypic behaviour. As a result, the Mg- and F-dominant minerals magniotriplite and wagnerite can no longer be considered polymorphs of Mg2PO4F, i.e., there is no basis for recognizing them as distinct species. Given that wagnerite has priority (1821 vs. 1951), the name magniotriplite should be discarded in favour of wagnerite. Hydroxylwagnerite, end-member Mg2PO4OH, occurs in pyrope megablasts along with talc, clinochlore, kyanite, rutile and secondary apatite in two samples from lenses of pyrope–kyanite–phengite–quartz-schist within metagranite in the coesite-bearing ultrahigh-pressure metamorphic unit of the Dora-Maira Massif, western Alps, Vallone di Gilba, Val Varaita, Piemonte, Italy. Electron microprobe analyses of holotype hydroxylwagnerite and of the crystal with the lowest F content gave in wt%: P2O5 44.14, 43.99; SiO2 0.28, 0.02; SO3 –, 0.01; TiO2 0.20, 0.16; Al2O3 0.06, 0.03; MgO 48.82, 49.12; FeO 0.33, 0.48; MnO 0.01, 0.02; CaO 0.12, 0.10; Na2O 0.01, –; F 5.58, 4.67; H2O (calc) 2.94, 3.36; –O = F 2.35, 1.97; Sum 100.14, 99.98, corresponding to (Mg1.954Fe0.007Ca0.003Ti0.004Al0.002Na0.001)Σ=1.971(P1.003Si0.008)Σ=1.011O4(OH0.526F0.474)Σ=1 and (Mg1.971Fe0.011Ca0.003Ti0.003Al0.001)Σ=1.989(P1.002Si0.001)Σ=1.003O4(OH0.603F0.397)Σ=1, respectively. Due to the paucity of material, H2O could not be measured, so OH was calculated from the deficit in F assuming stoichiometry, i.e., by assuming F + OH = 1 per formula unit. Holotype hydroxylwagnerite is optically biaxial (+), α 1.584(1), β 1.586(1), γ 1.587(1) (589 nm); 2V Z(meas.) = 43(2)°; orientation Y = b. Single-crystal X-ray diffraction gives monoclinic symmetry, space group P21/c, a = 9.646(3) Å, b = 12.7314(16) Å, c = 11.980(4) Å, β = 108.38(4) , V = 1396.2(8) Å3, Z = 16, i.e., hydroxylwagnerite is the OH-dominant analogue of wagnerite [β-Mg2PO4(OH)] and a high-pressure polymorph of althausite, holtedahlite, and α- and ε-Mg2PO4(OH). We suggest that the group of minerals related to wagnerite, triplite and triploidite constitutes a triplite–triploidite super-group that can be divided into F-dominant phosphates (triplite group), OH-dominant phosphates (triploidite group), O-dominant phosphates (staněkite group) and an OH-dominant arsenate (sarkinite). The distinction among the three groups and a potential fourth group is based only on chemical features, i.e., occupancy of anion or cation sites. The structures of these minerals are all based on the average triplite structure, with a modulation controlled by the ratio of Mg, Fe2+, Fe3+ and Mn2+ ionic radii to (O,OH,F) ionic radii.

Improving Surveying Accuracy and Efficiency in Connecticut: An Accuracy Assessment of GEOID03 and GEOID09

Comparing published NAVD 88 Helmert orthometric heights of First-Order bench marks against GPS-determined orthometric heights showed that GEOID03 and GEOID09 perform at their reported accuracy in Connecticut. GPS-determined orthometric heights were determined by subtracting geoid undulations from ellipsoid heights obtained from a network least-squares adjustment of GPS occupations in 2007 and 2008. A total of 73 markers were occupied in these stability classes: 25 class A, 11 class B, 12 class C, 2 class D bench marks, and 23 temporary marks with transferred elevations. Adjusted ellipsoid heights were compared against OPUS as a check. We found that: the GPS-determined orthometric heights of stability class A markers and the transfers are statistically lower than their published values but just barely; stability class B, C and D markers are also statistically lower in a manner consistent with subsidence or settling; GEOID09 does not exhibit a statistically significant residual trend across Connecticut; and GEOID09 out-performed GEOID03. A "correction surface" is not recommended in spite of the geoid models being statistically different than the NAVD 88 heights because the uncertainties involved dominate the discrepancies. Instead, it is recommended that the vertical control network be re-observed.

Age model and color measurements of sediment cores from the eastern equatorial Pacific

High-resolution records of glacial-interglacial variations in biogenic carbonate, opal, and detritus (derived from non-destructive core log measurements of density, P-wave velocity and color; r >= 0.9) from 15 sediment sites in the eastern equatorial (sampling resolution is ~1 kyr) clear response to eccentricity and precession forcing. For the Peru Basin, we generate a high-resolution (21 kyr increment) orbitally-based chronology for the last 1.3 Ma. Spectral analysis indicates that the 100 kyr cycle became dominant at roughly 1.2 Ma, 200-300 kyr earlier than reported for other paleoclimatic records. The response to orbital forcing is weaker since the Mid-Brunhes Dissolution Event (at 400 ka). A west-east reconstruction of biogenic sedimentation in the Peru Basin (four cores; 91-85°W) distinguishes equatorial and coastal upwelling systems in the western and eastern sites, respectively. A north-south reconstruction perpendicular to the equatorial upwelling system (11 cores, 11°N-°3S) shows high carbonate contents (>= 50%) between 6°N and 4°S and highly variable opal contents between 2°N and 4°S. Carbonate cycles B-6, B-8, B-10, B-12, B-14, M-2, and M-6 are well developed with B-10 (430 ka) as the most prominent cycle. Carbonate highs during glacials and glacial-interglacial transitions extended up to 400 km north and south compared to interglacial or interglacial^glacial carbonate lows. Our reconstruction thus favors glacial-interglacial expansion and contraction of the equatorial upwelling system rather than shifting north or south. Elevated accumulation rates are documented near the equator from 6°N to 4°S and from 2°N to 4°S for carbonate and opal, respectively. Accumulation rates are higher during glacials and glacial-interglacial transitions in all cores, whereas increased dissolution is concentrated on Peru Basin sediments close to the carbonate compensation depth and occurred during interglacials or interglacial-glacial transitions.

CO2 and vitamin B12 interactions determine bioactive trace metal requirements of a subarctic Pacific diatom

Phytoplankton growth can be limited by numerous inorganic nutrients and organic growth factors. Using the subarctic diatom Attheya sp. in culture studies, we examined how the availability of vitamin B(12) and carbon dioxide partial pressure (pCO(2)) influences growth rate, primary productivity, cellular iron (Fe), cobalt (Co), zinc (Zn) and cadmium (Cd) quotas, and the net use efficiencies (NUEs) of these bioactive trace metals (mol C fixed per mol cellular trace metal per day). Under B(12)-replete conditions, cells grown at high pCO(2) had lower Fe, Zn and Cd quotas, and used those trace metals more efficiently in comparison with cells grown at low pCO(2). At high pCO(2), B(12)-limited cells had ~50% lower specific growth and carbon fixation rates, and used Fe ~15-fold less efficiently, and Zn and Cd ~3-fold less efficiently, in comparison with B(12)-replete cells. The observed higher Fe, Zn and Cd NUE under high pCO(2)/B(12)-replete conditions are consistent with predicted downregulation of carbon-concentrating mechanisms. Co quotas of B(12)-replete cells were 5- to 14-fold higher in comparison with B(12)-limited cells, suggesting that >80% of cellular Co of B(12)-limited cells was likely from B(12). Our results demonstrate that CO(2) and vitamin B(12) interactively influence growth, carbon fixation, trace metal requirements and trace metal NUE of this diatom. This suggests the need to consider complex feedback interactions between multiple environmental factors for this biogeochemically critical group of phytoplankton in the last glacial maximum as well as the current and future changing ocean.

Lowering blood homocysteine with folic acid based supplements: meta-analysis of randomised trials

Objective: To determine the size of reduction in homocysteine concentrations produced by dietary supplementation with folic acid and with vitamins B-12 or B-6.

1993 University of Michigan Baseball Team

<b>Back Row:b> (10) Groundskeeper Erich Keil, Scott Niemiec, Scott Weaver, Mark Temple, Andy Wade, Brian Simmons, John Arvai, Matt Humbles, Student Manager Matt Hyde, Student Trainer Ann Whittenbach.

<b>Middle Row:b> (12) Volunteer Assistant Coach Ed Turek, Jasen Livingston, Chris Newton, Heath Murray, Nate Holdren, Matt Ferullo, Ray Ricken, Chad Chapman, Sean Coston, Ryan Van Oeveren, Rodney Goble, Trainer Rex Thompson.

<b>Front Row:b> (11) (from left): Assistant Coach Ace Adams, Toby Brzoznowski, Bryan Santo, Eric Heintschel, Co-Captain Todd Marion, Head Coach Bill Freehan, Co-Captain Scott Timmerman, Scott Winterlee, Matt Copp, Pat Maloney, Assistant Coach Dan O'Brien.

1998 University of Michigan Baseball Team

<b>4th Row:b> (12) Nick Alexander, Jeff Van Sickle, Mike Seestedt, David Parrish, Rob Bobeda, J.J. Putz, Bryan Cranson, Joe Young, Brian Berryman, John Papp, Ryan Kelley, Vince Pistilli.

<b>3rd Row:b> (12) Trainer Rex Thompson, Jason Alcaraz, Pete Martay, Brian Bush, Robbie Reid, Matt Herr, Luke Bonner, Mike Haskell, Bryce Ralston, Bobby Scales, Dan Sanborn, Student Trainer Rich Wright.

2nd Row (12) Derek Besco, Mario Garza, Jr., Mike Hribernik, Tyler Steketee, Brian Steinbach , Assistant Coach Chris Harrison, Head Coach Geoff Zahn, Assistant Coach Matt Hyde, Brian Kalczynski, Mick Kalahar, Mike Cervenak, Bryan Besco.

<b>Front Row:b> (11, Sitting) Student Manager Josh Taft, Seth Greene, Kevin Quinn, Bill LaRosa, Scott Tousa, C.J. Ghannam, Stephen Lenick, Andy Hood, Mike Norkus, Student Manager Jeff Singer, Groundskeeper Erich Keil.

1999 University of Michigan Baseball Team

<b>4th Row:b> (12) Trainer Joel Pickerman, Nick Alexander, Vince Pistilli, Nate Wright, Kirk Taylor, Phil Lorbert, Jeff Trzos, Nick Bellows, Joe Young, Jeff Sandor, Mike Sokol, Student Trainer Jaye Peterson.

<b>3rd Row:b> (12) Rob Bobeda, David Parrish, Bryan Cranson, Dan Sanborn, John Papp, Robbie Reid, Luke Bonner , Ryan Kelly, Pete Martay, Andy Hood, Bryce Ralston, Student Trainer Todd Sonquist.

2nd Row (11) Mike Seestedt, Brian Bush, Jason Alcaraz, Mike Cervenak, Assistant Coach Chris Harrison, Head Coach Geoff Zahn, Assistant Coach Matt Hyde, Assistant Coach John Edman, Bobby Scales, J.J. Putz, Bryan Besco.

<b>Front Row:b> (10, Sitting) Student Manager Josh Taft, Bobby Korecky, Jay Dines, Scott Tousa, C.J. Ghannam, Kevin Quinn, Bill LaRosa, Dan Dombos, Aaron Wilkens, Student Manager Jeff Singer.

2005 University of Michigan Baseball Team

<b>Top Row:b> (10) Brad Seddon, Michael Powers, Ben Jenzen, Andrew Hess, Derek VanBuskirk, Chris Fetter, Jeff N Tim Kalczynski, Alex Martin, Matt Petry.

<b>3rd Row:b> (12) Student Manager Sam Grossman, A.J. Scheidt, Chris Getz, Leif Mahler, Derek Feldkamp, Dre Ali Husain, Craig Murray, Dan Lentz, Mike Schmidt, Student Manager Chris Clark.

<b>2nd Row: b>(11) Jeff Kunkel, Jim Brauer, Michael Penn, Assistant Coach Scott Kingston, Assistant Coach Bo Head Coach Rich Maloney, Assistant Coach Jake Boss Jr., Kyle Bohm, Matt Butler, Phil Tognetti, Paul Hammond.

<b>Front Row:b> (6, Sitting) Alan Ulrich, Matt Rademacher, Kyle Miller, Doug Pickens, Eric Rose, Brad Roblin.

Histoire universelle de Diodore de Sicile /

Mode of access: Internet.

La science des personnes de cour, d'epée et de robe /

Mode of access: Internet.