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Djin L Tay,1 Lau C Thygesen,2 Elissa Kozlov,3 Katherine A Ornstein4 1College of Nursing, University of Utah, Salt Lake City, UT, USA; 2National Institute of Public Health, University of Southern Denmark, Copenhagen, Denmark; 3Department of Health Behavior, Society and Policy, School of Public Health, Rutgers, The State University of New Jersey, Piscataway, NJ, USA; 4School of Nursing, Johns Hopkins University, Baltimore, MD, USACorrespondence: Djin L Tay, College of Nursing, University of Utah, 10S 2000 E, Salt Lake City, UT, 84112, USA, Tel +1 801-882-3037, Email Djin.Tay@nurs.utah.eduPurpose: The death of a close family member is commonly accompanied by intense grief, stress, and loss of social support. We hypothesized that recent bereavement would be associated with an increase in symptom exacerbations among adults with serious mental illness (SMI) whose partners or parents had died.Patients and Methods: Adults whose partners and parents had died in Denmark between January 1, 2010, and June 30, 2016, were identified using linked population-based registries. History of SMI was defined as having a diagnosis of schizophrenia and schizoaffective disorders, major depression, and bipolar disorder in the five years preceding their family member’s death in the Danish Psychiatric Central Research Register using International Classification of Diseases-10 codes. The odds of SMI exacerbation (ie, attempt or completion of suicide or psychiatric hospitalization) among partners and children in the first two years after death in 3-month intervals were estimated with generalized estimating equations.Results: 12.8% of partners and 15.0% of adult children with a history of SMI experienced any SMI exacerbation two years after bereavement. Among bereaved partners, older age (80+ years) was associated with a lower risk of experiencing an SMI exacerbation compared with partners aged 18– 49 years (ORadj=0.29, [0.18– 0.45]). Partners with a history of SMI had significantly increased odds of SMI exacerbations three months after their partners’ death compared to prior to their partners’ death (ORadj = 1.43, [1.13– 1.81]). There was no evidence that adult children with SMI experience increased SMI exacerbations after the death of their parents compared to prior to death.Conclusion: Adults with a history of SMI whose partners had died are at increased risk for an SMI exacerbation post bereavement. Additional bereavement resources and support should be provided to those with a history of SMI, especially in the period immediately after death.Keywords: severe mental disorders, bereavement, population register, suicide, emergency psychiatric services

The Sallanlatva massif belongs to the group of Paleozoic alkaline-ultrabasic complexes wide spread in the Kola Region (the northwestern part of the Fennoscandian Shield). In the central part of this massif, the host ijolite and urtites contain calcite, ankerite, ankerite-dolomite and siderite carbonatites. The explosive processes that led to the formation of carbonatite breccias in the calcite and ankerite-dolomite carbonatites occurred in Sallanlatva massife in the last stages of the carbonatite magmatism. There are two types of explosive carbonatite breccias in the Sallanlatva massif: (1) glimmerite-calciocarbonatite breccias, and (2) siderite-dolomite breccias. Analysis of the mineral composition of fragments and matrix and the shape of fragments in breccias has shown that the first material to intrude into the host calcite and ankerite-dolomite carbonatites was calcite melt. After that, dolomite melt penetrated through the fracture zones, which resulted in the formation of siderite-dolomite breccias. The differences in the mineral composition of the breccia matrix suggest that the residual carbonatite melts originate from separate magma chambers. The chamber with calcite melt was located at great depth, and some captured glimmerite fragments were abraded during the melt upwelling. Silicate-dolomite melts lifted from a shallower depth; the captured fragments of siderite carbonatites retained their angular shape. Late hydrothermal processes yielded veins and caverns with Ba-Sr-P-S-Ti-REE mineralization in the breccias and host rocks.

The objects of the study are apocarbonatitic titanium metasomatites ("titanium carbonatites") associated with the rare earth carbonatites of the Petyayan-Vara area of the Vuoriyarvi complex (the Kola region). In this paper, the following mechanism for the formation of these rocks has been substantiated based on the agreed results of mineralogical and geochemical studies. Prior to the onset of carbonatite genesis, a fluorine-enriched fluid phase originated in the lower horizons of the complex passed along the deep-permeating fracture system of several hundred meters length up to the level of the modern erosion surface. It transported Al, Fe2+, Mg, Ti, P into the pyroxenites and Si, Ca and Na out of them, as a result of which the pyroxenites were transformed into giant-grained phlogopite rocks – glimmerites. The most probable source of this fluid is alkaline aluminosilicate magma. Then carbonate melts intruded along the same fractures. In the course of carbonatite genesis, F-fluid caused a local migration of K, Al, Si, Fe, P, Ti, Nb, Ta, Zr, Hf and HREE out of glimmerites into igneous dolomite carbonatites, which led to the formation of apocarbonatitic titanium metasomatites. They represent several paragenetic associations superimposed on each other, the mineral composition and the formation sequence of which correspond to the metasomatic column zones directly observed within the contact "carbonatite – altered pyroxenite". The separation of HFSE and REE is controlled by the same metasomatic column: Ti, Nb and Ta were accumulated in titanium carbonatites, i. e. in associations of the frontal and intermediate zones, and Zr, Hf and HREE – in apatitized fields corresponding to the rear zone of the column. Accordingly, the fractionation of these elements occurred due to the "fluid – rock" interaction. Subsequently, the same long-lived fractures served as a channel for REE-Sr-Ba-S fluids, but the recrystallization caused by K-Al-Si-Ti-F-metasomatism made titanium carbonatites dense and fine-grained in texture, what, in most cases, "protected" these rocks from the influences of later processes.

The results of complex petro-mineragraphic, Raman and isotope- geochemical study of three types of graphite- bearing rocks circulated at different distances from the alkaline granites: (1) kyanite schists of Bolshiye Keivy, sampled at a considerable distance from a contact with alkaline gran ites; (2) sillimanite schists, sampled close to the contact, and (3) silexites, located in the inner part of th e alkaline granite massif Western Keivy have been presented. Five morphogenetic types of graphite have been revealed in the rocks under consideration: fine- grained Gr-1, intergranular Gr-2, nest-shaped Gr-3, vein Gr- 4 and spherulitic Gr-5. Current study demonstrates that these five types of graphite distinctly vary not only i n morphology, but also in temperature of crystallization, as determined by RSCM-Raman geothermometer, and in carbon isotop e composition. The most likely source for the anomalous "light" graphite Gr-1 and Gr-2 [δ 13 C(PDB) = −43...−45 ‰] from kyanite schists is a water- methane fluid originating from sedimentary rocks with org anic compounds. The carbon of graphite Gr-5 of the silexites selected at the inner part of alkaline granite massif West ern Keivy, on the contrary, proved to be most "heavy" [δ 13 C(PDB) = −8 ‰], which indicates its origin from the lower crustal or mantle carbon dioxide fluid. Thus, carbon extracted into the rocks of Keivy structure from at least two contrasting isotope sources. Graphite Gr-3, that makes up the bulk of graphite of exocontact sil limanite schists, is also isotopically light, but not anomalously [δ 13 C(PDB) = −17...−28 ‰]. The crystallization temperature of the gi ven graphite (435−520 ºC), and its structural relationships with other minerals of th e rock evidence of its synmetamorphic origin. The presence of veinlets of isotopically heavy [δ 13 C(PDB) = −10 ‰...−11 ‰] high-temperature (570−670 ºC) graphite intersecting minerals of the metamorphic paragenesis (i ncluding Gr-3) indicates that the introduction of the granites occurred into the previously metamorphosed strat a and was accompanied by thermal and fluid influence on these strata.