ABSTRACT Collembola are known to feed on soil fungi, mycorrhizae and plant derived products. A recent study revealed that one species of Collembola, Protaphorura fimata, completely switched from decomposer to herbivore when live roots were present. The current study investigated the occurrence of diet-switching in Folsomia candida Willem. from plant detritus to live by examining its dietary preferences using stable isotope techniques. They were offering with live maize roots (C4 plant) in C3 soil, along with 15N enriched ryegrass litter and. Results demonstrated the presence of a partial diet-switch from detritus to live maize roots. Additional tests suggested that the diet-switch towards maize roots was a response to both improved food quality and greater food availability. The presence of live roots improved the body growth of F. candida and the incorporation of C from live roots into Collembola tissue suggesting

nÃo hà / Este trabalho descreve a composiÃÃo quÃmica das espÃcies marinha Palythoa caribaeorum e Protopalythoa variabilis, coletadas no municÃpio de Paracuru-CE. O fracionamento cromatogrÃfico do extrato hexÃnico de P. caribaeorum, resultou no isolamento de quatro esterÃides tetracÃclico de esqueleto ergostano: 24(R)-ergost-5-en-3-ol (P-1); 5,8-epidioxi-24(R)-ergost-6-en-3-ol (P-2); 24(R)-ergost-5-en-3,7-diol (P-4) e 24(R)-7-hidroperoxi-ergost-5-en-3-ol (P-7), um derivado do glicerol, 1-O-hexadecilglicerol (P-3) e quatro ceramidas: N-(2S,3R,4E,8E,1,3-dihidroxi-4,8-octadecadieno)hexadecanamida (P-5); N-(2S,3R,4E,1,3-dihidroxi-4-octadeceno)-hexadecanamida (P-6), N-[2S,3R,4E,8E,1-(2â-metilamino-etanosulfonila)-3-hidroxi-4,8-octadecaÂdieno]hexadecanamida (P-8) e N-[2S,3R,4E,1-(2â-metilaminoetano-sulfonila)-3-hidroxi-4-octadeceno]hexadecanamida (P-9). Do fracionamento cromatogrÃfico do extrato etanÃlico, foi possÃvel isolar o esterÃide 24(R)-ergost-7-en-3,56-triol (P-10) e o nucleosÃdeo 2-metil-timidina (P-11). Do estudo quÃmico do extrato hexÃnico de P. variabilis obteve-se os mesmos constituintes quÃmicos isolados de P. caribaeorum (P-1, P-2, P-3 e P-4) e as quatro ceramidas (P-5, P-6, P-8 e P-9). AlÃm destes compostos foi isolado um Ãster de cadeia alifÃtica, hexadecanoato de nonila (P-12) e o esterÃide Ãcido 24(R)-B-norergostan-3-5-diol-6-carboxÃlico (P-13). O potencial citotÃxico e antifÃngico das ceramidas foi avaliado, entretanto, estas nÃo apresentaram atividade. Os compostos foram isolados atravÃs de cromatografia de adsorÃÃo em gel de sÃlica e cromatografia lÃquida de alta eficiÃncia. As estruturas dos compostos obtidos foram elucidadas utilizando tÃcnicas espectroscÃpicas e espectromÃtricas, tais como: espectrometria de massa acoplada a cromatografia gasosa (CG/EM); espectrometria de massa de alta resoluÃÃo (EMAR); espectroscopia na regiÃo do infravermelho (IV) e RessonÃncia MagnÃtica Nuclear (RMN 1H, 13C e 15N) atravÃs de sequÃncias de pulsos uni e bidimensionais e comparaÃÃo com dados de RMN na literatura. / This work describes the chemical composition of the marine species Palythoa caribaeorum and Protopalythoa variabilis, both collected at Paracuru beach, state of CearÃ. The cromatographic fractionation of the hexane extract from P. caribaeorum resulted in the isolation of four tetracyclic sterols possessing the ergostan skeleton: 24(R)-ergost-5-en-3b-ol (P-1); 5 a,8a-epidioxy-24(R)-ergost-6-en-3b-ol (P-2); 24(R)- ergost-5-en-3b,7a-diol (P-4) and 24(R)-7a-hydroperoxy-ergost-5-en-3b-ol (P-7), a glycerol derivative, 1-O-hexadecylglycerol (P-3) and four ceramides: N- (2S,3R,4E,8E,1,3-dihydroxy-4,8-octadecadienyl)hexadecanamide (P-5); N- (2S,3R,4E,1,3-dihydroxy-4-octadecenyl)hexadecanamide (P-6); N-[2S,3R,4E,8E,1-(2â- methylamino-ethanosulfonyl)-3-hydroxy-4,8-octadecaenyl]hexadecanamide (P-8) and N-[2S,3R,4E,1-(2â-methylaminoethano-sulfonyl)-3-hydroxy-4-octadecenyl]hexadecanamide (P-9). The cromatographic fractionation of the ethanol extract permited the isolation of a steroid, 24(R)-ergost-7-en-3b,5a,6b-triol (P-10) and a nucleoside 2- methyltimidine (P-11). Column chromatography of the hexane extract of P. variabilis led to the isolation of nonyl hexadecanoate (P-12), the sterol 24(R)-B-norergostan-3b- 5b-diol-6b-carboxylic acid (P-13) and the same chemical constituents previously isolated from P. caribaeorum (P-1, P-2, P-3 e P-4) including the four ceramides (P-5, P-6, P-8 e P-9). The citotoxic and antifungal properties of all ceramides were evaluated, nevertheless none of them showed any activity. All compounds were isolated through adsorption column cromatography over silica gel followed by high performance liquid chromatography. The structures of the isolated compounds were elucidated using spectrometric techniques, such as: GC/MS, HRESIMS, IR and NMR (1H, 13C and 15N) through 1D and 2D pulse sequences and, whenever the case, comparison with literature data

Some endophytes in mutualistic associations with Festuca, Lolium and other grass species produce insecticidal loline alkaloids (1-aminopyrrolizidines; LA). These loline alkaloids have a saturated pyrrolizidine ring system (two-rings sharing a carbon and nitrogen atom), a 1-amine substituted with methyl, acetyl, or formyl groups, and an oxygen bridge between C-2 and C-7. The development of a reliable system of production of LA in cultures of the Lolium pratense (meadow fescue) endophyte, Neotyphodium uncinatum, facilitated work on the LA biosynthetic pathway. N. uncinatum produced norloline, loline, methylloline, N-acetylnorloline (NANL), N-formylloline (NFL), and N-acetylloline as detected in culture filtrates. The total production of the two most abundant alkaloids, NANL and NFL, approached 1000 g ml-1 of fungal filtrate. 1H and 13C chemical shifts were previously reported for this group of alkaloids. Extraction and synthesis of sufficient quantities of the alkaloids allowed determination of previously unknown 15N chemical shifts of some LA. Knowledge of 13C and 15N chemical shifts allowed identification of precursors by feeding stable-isotope-labeled compounds. Initially, due to structural similarity to other plant pyrrolizidines, this study examined putrescine and spermidine as possible precursors to LA. Feeding of 14C putrescine to the fungal cultures failed to demonstrate any enrichment in the LA, but enriched spermidine. In contrast, cultures fed with positionally labeled 2H, 13C and 15N amino acids namely, L-ornithine, L-proline, L-aspartate, L-homoserine, and L-methionine demonstrated specific isotopic enrichment in NFL. Determination of the enrichment from the labeled amino acids utilized 13C and 15 N NMR (nuclear magnetic resonance) and gas chromatography-mass spectroscopy (GC-MS). This study allowed the biosynthetic origins of all carbons and nitrogens of NFL to be determined. NFL incorporated L-proline into the B-ring and L-homoserine into the A-ring and 1-amine. The results strongly indicated that polyamines are not precursors of LA and implicated a novel biochemical pathway for the synthesis of LA.

Submitted by Alice Araujo (alice.caraujo@ufpe.br) on 2018-06-20T17:52:58Z No. of bitstreams: 2 license_rdf: 811 bytes, checksum: e39d27027a6cc9cb039ad269a5db8e34 (MD5) TESE Kennedy Nascimento de Jesus.pdf: 2821633 bytes, checksum: ad7413c76f1a1fd792f8d226e55211d0 (MD5) / Made available in DSpace on 2018-06-20T17:52:58Z (GMT). No. of bitstreams: 2 license_rdf: 811 bytes, checksum: e39d27027a6cc9cb039ad269a5db8e34 (MD5) TESE Kennedy Nascimento de Jesus.pdf: 2821633 bytes, checksum: ad7413c76f1a1fd792f8d226e55211d0 (MD5) Previous issue date: 2017-02-02 / CAPES / A conversão de áreas de vegetação nativa em áreas destinadas à exploração agropecuária é apontada como um dos principais fatores responsáveis pelas emissões de Gases de Efeito Estufa para a atmosfera. Essas mudanças no uso da terra causam na paisagem um mosaico de áreas com diferentes usos e coberturas do solo. Porém, ainda é limitado o conhecimento da dinâmica do carbono (C) e do Nitrogênio (N) do solo nesses sistemas, principalmente na região Nordeste do Brasil. Nesse sentido, o objetivo desse trabalho foi determinar as alterações dos estoques e da dinâmica do C e N no solo devido às mudanças de uso da terra nas diferentes regiões fisiográficas e nas principais classes de solo de Pernambuco. Foram realizados três estudos, que auxiliaram no alcance do objetivo proposto: 1) no primeiro, foi realizado um levantamento e compatibilização da literatura sobre os estoques de C na camada superficial (0-30 cm) dos solos de Pernambuco. 2) no segundo estudo, foram quantificados os estoques de carbono (in situ) e sua distribuição nas camadas ao longo do perfil do solo (0-100 cm) em áreas de vegetação nativa, agrícolas e pasto, nas principais regiões fisiográficas e classes de solo do Estado; e 3) no terceiro, foram avaliados a dinâmica do C e do N, através da abundância natural de δ13C e δ15N e das concentrações de C e N em perfis (0-100 cm) de Argissolos ao longo de um gradiente climático em Pernambuco em áreas representativas de floresta nativa, de pasto e agrícolas. Em todos os estudos, as áreas de vegetação nativa foram tomadas como condição original do solo de acordo com cada região estudada. Nos estudos 2 e 3 quantificou-se as concentrações de C e N por meio de analisador elementar CHN e no estudo 3 foram quantificadas a abundância natural de δ 13C e δ 15N nos Argissolos do Estado, por meio de espectrômetro de massa. Aproximadamente 368 Tg de C estão estocados nos solos de Pernambuco de 0-30 cm. De uma forma geral, os maiores estoques de carbono total ocorreram nas vegetações nativas densas e decresceram da região úmida à semiárida Oeste, com grandes variações entre as classes de solos. A substituição da vegetação nativa para implantação de áreas de pastagens ou agrícolas acarretou mudanças no sinal δ13C do solo, sendo maiores nas áreas úmidas e subúmidas do estado em relação às áreas semiáridas. O enriquecimento de δ15N encontrado na superfície do solo das regiões semiáridas em relação às áreas úmidas e subúmidas estão associados as menores concentrações de C e N presentes nos Argissolos dessa região, em decorrência das maiores temperaturas e menores precipitações pluviais. Fica evidente que a intervenção humana nessas áreas através de práticas agropecuárias, reduz os estoques e modificam a dinâmica do C e do N no solo, e para se contrapor a esta situação no Estado, são necessárias medidas mitigatórias, como a adoção de sistemas conservacionistas do solo e da água, através de políticas públicas de incentivo às práticas conservacionistas em substituição à agricultura de baixo C. / The conversion of native vegetation areas into agricultural areas is pointed out as one of the main factors responsible for the emissions of greenhouse gases to the atmosphere. Changes in land use create a mosaic of areas in the landscape with different soil coverages and knowledge of the dynamics of C and N in these systems is limited. The objective of this work was to determine the changes in soil carbon (C) and nitrogen (N) stocks and dynamics due to changes in land use in the different physiographic regions and in the main soil classes of Pernambuco state. Three studies were carried out: 1) the first was a survey and compatibilization of the literature on C stocks in the surface layer (0-30 cm) of the soils of Pernambuco; 2) the second study was a quantification of the C stocks along the different layers of the soil profile (0-100 cm) in areas under native vegetation, agriculture and pasture, in the main physiographic regions and soil classes of Pernambuco; and 3) the third study evaluated soil C and N dynamics through the natural abundance of δ13C and δ15N and the concentrations of C and N in profiles of Ultisols (0-100 cm) along a climatic gradient in Pernambuco. In all studies, dense native vegetation areas were taken as the original, reference soil condition. In studies 2 and 3 the concentrations of C and N were quantified using CHN elemental analyzer. In study 3 the natural abundance of δ13C and δ15N were quantified by mass spectrometer. Approximately 368 Tg of carbon are stored in the soils of Pernambuco in the 0-30 cm layer. The largest total carbon stocks occurred under dense native vegetation and decreased from the humid region towards the semi-arid western state region, with large variations among soil classes. The replacement of the native vegetation by agriculture or pasture caused changes in the soil δ13C signal, being greater in the humid areas and subhumid regions than in the semi-arid region. The enrichment of δ15N in the soil surface layer of the semi-arid regions in relation to the humid and subhumid regions is associated with the lower concentrations of C and N in these regions, due to their higher temperatures and lower rainfall. It is evident that Human intervention in these areas through conventional farming practices reduces soil carbon stocks at levels lower than those found in native areas, and modifies the C and N dynamics in the soil in these regions. To counteract this situation in the State, mitigating measures are necessary, such as the adoption of soil and water conservation systems, through public policies to encourage conservation practices in place of low carbon agriculture.

Data de aprova??o retirada da vers?o impressa do trabalho. / ?rea de concentra??o: Produ??o Vegetal. / Submitted by Jos? Henrique Henrique (jose.neves@ufvjm.edu.br) on 2018-08-14T22:18:43Z No. of bitstreams: 2 license_rdf: 0 bytes, checksum: d41d8cd98f00b204e9800998ecf8427e (MD5) camila_rodrigues_costa.pdf: 5661319 bytes, checksum: b9deab885dfc53d90534a8a979f8d00d (MD5) / Approved for entry into archive by Rodrigo Martins Cruz (rodrigo.cruz@ufvjm.edu.br) on 2018-10-05T19:35:26Z (GMT) No. of bitstreams: 2 license_rdf: 0 bytes, checksum: d41d8cd98f00b204e9800998ecf8427e (MD5) camila_rodrigues_costa.pdf: 5661319 bytes, checksum: b9deab885dfc53d90534a8a979f8d00d (MD5) / Made available in DSpace on 2018-10-05T19:35:26Z (GMT). No. of bitstreams: 2 license_rdf: 0 bytes, checksum: d41d8cd98f00b204e9800998ecf8427e (MD5) camila_rodrigues_costa.pdf: 5661319 bytes, checksum: b9deab885dfc53d90534a8a979f8d00d (MD5) Previous issue date: 2018 / Funda??o de Amparo ? Pesquisa do estado de Minas Gerais (FAPEMIG) / As turfeiras s?o ambientes de transi??o entre os ecossistemas terrestres e aqu?ticos, formados pela acumula??o sequencial de mat?ria org?nica. Extremamente sens?veis as mudan?as nos padr?es de precipita??o e temperatura, as turfeiras s?o consideradas verdadeiros arquivos da evolu??o do ambiente ao seu redor. Nas depress?es das ?reas dissecadas da Serra do Espinha?o Meridional, Minas Gerais, ocorrem ambientes propicios para forma??o de turfeiras. Dentre elas encontra-se a turfeira do Rio Preto (18?14'5,25"S e 43?19'7,24" WGS, 1.593 m.s.m) inserida no Parque Estadual do Rio Preto. A turfeira do Rio Preto ? colonizada por diferentes fisionomias do Bioma Cerrado principalmente o Campo ?mido e Campo Rupestre, sendo encontrados ainda redutos de Floresta Estacional Semidecidual (Cap?es de Mata). O objetivo deste trabalho foi reconstituir as mudan?as paleoambientais ocorridas desde o final do Pleistoceno Tardio. Para isto foi utilizada uma abordagem multi-proxy, consistindo em estratigrafia do perfil do solo da turfeira, an?lises palinol?gicas, de is?topos est?veis (13C e 15N), de composi??o geoqu?mica e data??es radiocarb?nicas. A idade mais antiga, obtida da base do testemunho, foi de 23.037 anos cal. AP, indicando que a forma??o da turfeira se deu a partir do Pleistoceno Tardio. A partir da an?lise conjunta dos proxys foi poss?vel inferir cinco principais fases de mudan?as paleoambientais: RP-I, entre ~ 23.037 e 13.500 anos cal. AP, clima bastante ?mido e frio, possibilitando a presen?a de indicadores de Floresta Montana e o empobrecimento do sinal isot?pico. Este foi um per?odo de bastante instabilidade na bacia hidrogr?fica da turfeira, inferida pelo alto teor de Si, indicador de sinal de material mineral local; RP-II, entre ~13.500 e 11.700 anos cal. AP, ligeiro aumento da temperatura e queda na umidade levando a redu??o de indicadores de clima frio e a expans?o da vegeta??o campestre. No entanto as condi??es ainda eram mais ?midas e frias que as atuais, e a ind?cios de diminui??o do sinal de material mineral local; RP-III, entre ~11.700 e 8.500 anos cal. AP, tend?ncia de aumento da temperatura e diminui??o da umidade em conjunto com a mudan?a da vegeta??o de plantas C3 para C4, causando a forte retra??o das Floresta Estacional Semidecidual e Floresta Montana, em conjunto aumento do fluxo de sinal de material mineral local; RP-IV, entre ~8.500 e 7.000 anos cal. AP, condi??es de clima ainda mais seco e quente, causando o desaparecimento dos indicadores de clima frio, retra??o do Campo ?mido e expans?o do Campo Rupestre. Per?odo de bastante estabilidade da bacia hidrogr?fica da turfeira, sugerido pelo baixo conte?do de material mineral; RP-V, de 7.000 anos cal. AP at? o presente, clima era novamente mais ?mido e temperaturas mais amenas, semelhante ?s condi??es atuais, aumento na acumula??o de turfa, possibilitando o reaparecimento dos indicadores de Floresta Montana e Floresta Estacional Semidecidual junto com a retra??o do Campo, e diminui??o da entrada de material mineral. Flutua??es no clima influenciaram fortemente as mudan?as na paleovegeta??o e na estrutura sedimentar do registro da turfeira do Rio Preto. Devido ? import?ncia das turfeiras, n?o s? como arquivo de mudan?as paleoambientais, mas tamb?m pelos seus servi?os ambientais (armazenamento de ?gua e de carbono), estes ambientes precisam ser melhores protegidos. / Disserta??o (Mestrado) ? Programa de P?s-Gradua??o em Produ??o Vegetal, Universidade Federal dos Vales do Jequitinhonha e Mucuri, 2018. / The peatlands are transitional environments between terrestrial and aquatic ecosystems, formed by the sequential accumulation of organic matter. Extremely sensitive to changes in precipitation and temperature patterns, peatlands are real archives of the evolution of the environment around them. In Serra do Espinha?o Meridional, Minas Gerais State, Brazil, in depressions of the dissected areas occurs an environment conducive to formation of peatlands. Among them the peatland of Rio Preto (18?14'5,25"S e 43?19'7,24" WGS, 1.593 m.s.m), located in the Rio Preto State Park. The area is colonized by different vegetation physiognomy of the Cerrado Biome, mainly Rupestre Fields and Wet Fields, beyond of redoubts of Semidecidual Stationary Forests, called Capon Forests. The area is colonized by different vegetation physiognomy of the Cerrado Biome, mainly Rupestre Fields and Wet Fields, beyond of redoubts of Semidecidual Stationary Forests, called Capon Forests. The objective of this work was to reconstruct the paleoenvironmental changes that have occurred since the Late Pleistocene. The work was constituted by the application of a multi-proxy approach, such as peatland soil stratigraphy, palynological analyzes, stable isotopes (13C and 15N), geochemical composition analyzes and 14C dating. The oldest age obtained at the base of the peatland profile was 23.037 cal. years BP, indicating that the formation of the peatland occurred during the Late Pleistocene. In this study it was possible to infer five main stages of paleoenvironmental changes: RP-I ~23.000-13.500 cal. years BP, very cold climate and very humid, presence of Montana Forest indicators and impoverishment of the isotopic signal, period of instability in hydrographic basin of the peatland; RP-II ~13.500-11.700 cal. years BP, small increase in temperature and decreased humidity, reduction of the indicators of cold climate and the expansion of the field vegetation, however the climatic conditions were more humid and cooler than the current, decrease of the entrance of local mineral material; RP-III ~11.700-8.500 cal. years BP, trend of increased temperature and decreased humidity, change in vegetation from C3 to C4 plants, reduction of the Semideciduous Seasonal Forest and Mountain Forests, increased flow of local mineral material; RP-IV ~8.500-7.000 cal. years BP, drier and hotter weather, causing the disappearance of the indicators of cold weather, retraction of the Wet Field and expansion of Rupestre Field. Period of very stability in the watershed of the peatland; RP-V 7.000 cal. years BP until present, increased humidity and decrease in temperature, as current conditions, increased accumulation of peat, reappearance of the indicators of Montana Forest and Seasonal Semideciduous Forest and retraction of the Field, decrease of regional and local dust. Fluctuations in the climate influenced changes in paleovegetation and the sedimentary structure of the peatland Rio Preto. Given the value of peatlands as archives of paleoenvironmental changes and their environmental functions, these environments need to be better protected.