Non-Gaussianity from Instant and Tachyonic Preheating

We study non-Gaussianity in two distinct models of preheating: instant and tachyonic. In instant preheating non-Gaussianity is sourced by the local terms generated through the coupled perturbations of the two scalar fields. We find that the non-Gaussianity parameter is given by $f_{NL}^{\phi}\sim 2g < O(1)$, where $g$ is a coupling constant, so that instant preheating is unlikely to be constrained by WMAP or Planck. In the case of tachyonic preheating non-Gaussianity arises solely from the instability of the tachyon matter and is found to be large. We find that for single field inflation the present WMAP data implies a bound $V_{0}^{1/4}/M_{P}\leq 10^{-4}$ on the scale of tachyonic instability. We argue that the tachyonic preheating limits are useful also for string-motivated inflationary models.Comment: 12 pages, 1 figure, additional discussion, improved constraint on the scale of tachyonic preheatin

Virulence factors of non-O1 non-O139 Vibrio cholerae Project in biotechnology with measurement systems, 12hp

Abstract Cholera is a medical condition caused by Vibrio cholerae. The most common symptoms of the disease are diarrhea, vomiting, oedema and dehydration. V. cholerae is also known to possess putative virulence factors such as hemagglutinin protease, hemolysin/cytolysin which may assist in bacterial detachment and/or host cell death. On the basis of presence of surface O-antigen, V. cholerae can be divided into different serogroups. Some belong to serogroup O1 or O139 while strains of serogroups other than these are collecctively known as non-O1 and non-O139 strains. Members of O1 and O139 serogroups are responsible for all known cholera endemics while those belonging to non-O1, non-O139 serogroups can occasionally cause gastro-intestinal or extra-intestinal illness and septicemia. The mechanisms for how O1, O139 V. cholerae cause cholera are known, while further studies on non-O1, non-O139 V. cholerae are needed. Study described in this report was made to detect virulence factors of six strains; C6706, L1, L4, USS, KI, and V5 belonging to different serogroups. The strains were tested for hemagglutination, proteolysis and hemolysis. We also tried to detect the presence of various virulence factor genes in these strains using polymerase chain reaction (PCR). PCR analysis showed the presence of hlyA (hemolysin), prtV and hapA (metalloproteases) genes in all the tested strains. Furthermore the PCR assays showed the absence of ctx (cholera toxin) gene in all the tested strains except V. cholerae strains C6706 and USS, both belonging to serogroup O1. All six strains showed hemolytic activity, hemagglutination and at least L1, L4, KI, USS and V5 exhibit proteolytic activity. The strains were also tested for serum resistance. The two O1 strains, namely C6706 and USS, did not survive in active blood serum while the non-O1, non-O139 strains had a survival rate of 51-97% in the active blood serum. Since the non-O1, non-O139 V. cholerae can survive in the blood serum, the blood might be a possible invasive pathway for these bacteria

Proterozoic crustal evolution in southcentral Fennoscandia

The Transscandinavian Igneous Belt (TIB) and the Eastern Segment of the Southwest Scandinavian Domain reflect advanced stages of continental growth within the Fennoscandian Shield. The relationship between the two units is not clear, mainly because N-S trending shear zones of the Protogine Zone transect the border zone. The main goal of this thesis has been to investigate rocks in the border zone and to conclude how these rocks differ from each other. In this work two volcanic sequences and 24 granitoids in the border area, near Jönköping, were examined. The thesis reports geochemical and Sm-Nd isotope data as well as U-Pb ion microprobe zircon dates for extrusive and intrusive rocks in the southwestern part of the TIB and intrusive rocks in the eastern part of the southern Eastern Segment. The TIB rocks are subdivided into TIB-0, TIB-1 and TIB-2 groups based on their ages. In this work, the Habo Volcanic Suite and the Malmbäck Formation are dated at 1795±13 Ma and 1796±7 Ma respectively, which establishes that they are part of the TIB-1 volcanic rocks. The Malmbäck Formation is situated in the southwestern part of TIB, east of the Protogine Zone, whereas the Habo Volcanic Suite is located c. 50 km northwest of the Malmbäck Formation, between shear zones of the Protogine Zone. Both suites comprise mafic to felsic components and the Malmbäck Formation includes one of the largest mafic volcanic rock units of the TIB-1. The Malmbäck Formation comprises fairly well preserved volcanic rocks, with primary textures, although mineral parageneses in some rocks suggest metamorphism at up to epidote-amphibolite facies conditions. Amphibolites facies metamorphism and deformation has largely obscured primary textures of the Habo Volcanic Suite. Dating of a Barnarp granite which intrudes the Habo Volcanic Suite gave an age of 1660±9 Ma, corresponding to TIB-2. The occurrences of Malmbäck Formation megaxenoliths within TIB-1 granitoids are explained by stoping. Geochemical signatures of the two metavolcanic rock suites suggest emplacement in an active continental margin setting. It is further suggested that the TIB regime was complex, similar to what is seen in the Andes today, with different regions characterised by subduction-related magmatism, Andinotype extension as well as local compression. Twenty-one granitoids (including the granite intruding the Habo Volcanic Suite), across and in the border zone between the TIB and the Eastern Segment, were dated by U-Pb zircon ion probe analysis. Eighteen of the granitoids yielded TIB-2 magmatic ages, ranging between 1710 and 1660 Ma. Eighteen granitoids were analyzed for geochemistry and Sm-Nd isotopes. The geochemical and isotopic signatures of the granitoids proved to be similar, supporting the theory that the TIB and the Eastern Segment originated from the same type of source and experienced the same type of emplacement mechanisms. Further, it is concluded that the TIB-2 granitoids, from both the TIB and the Eastern Segment, were derived by reworking of juvenile, pre-existing crust, in an essentially east- to northeast-directed subduction environment. The U-Pb zircon ion microprobe analyses also dated zircon rims which formed by metamorphism during the 1460-1400 Ma Hallandian-Danopolonian orogeny, in granitoids of both the southern Eastern Segment and the western TIB. Leucosome formation, for two samples was dated at 1443±9 Ma and 1437±6 Ma. An aplitic dyke, cross-cutting NW-SE to E-W folding and leucosome formation in the Eastern Segment was dated at 1383±4 Ma, which sets a minimum age for the NW-SE to E-W folding in the area. Hence, it is concluded that the leucosome formation and the NW-SE to E-W folding in the investigated part of the Eastern Segment as well as NW-SE to E-W penetrative foliation and lineation in the western TIB took place during the 1470-1400 Ma Hallandian-Danopolonian orogeny. No c. 970 Ma Sveconorwegian ages were recorded in any of the areas investigated. Nevertheless, Sveconorwegian (in addition to earlier) block movements caused uplift of the Eastern Segment relative to the TIB, revealing from west to east: (1) the highly exhumed metamorphosed southern Eastern Segment, in which the effects of both the Hallandian-Danopolonian and the Sveconorwegian orogenies can be seen, (2) the partly exhumed westernmost TIB-2 showing the effects of the Hallandian-Danopolonian orogeny only, and (3) the easternmost TIB-2 granitoids, as well as the supracrustal and shallow emplaced TIB-1 granitoid rocks in the east. The main part of TIB was apparently unaffected by the Hallandian-Danopolonian orogeny, apart from the intrusion of subordinate felsic bodies and mafic dykes. Tilting and other block movements within the Eastern Segment also occurred during the uplift, revealing lower crustal sections in the south compared to the northern part