Wyniki wyszukiwania - Biblioteka Nauki

1

Chiński rynek spożywczy a szanse polskiej żywności

100%

Gołębiowska B.

Przemysł Spożywczy

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2015

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tom T. 69, nr 9

2--5

PL

Po otwarciu na świat w 1978 r. rynek produktów spożywczych i struktura konsumpcji w Chinach bardzo się zmieniły. Europejscy producenci i eksporterzy muszą dostosować się do potrzeb chińskiego konsumenta. Polskie produkty spożywcze są już dostępne w sklepach Pekinu i Szanghaju, co zwiększa ich rozpoznawalność na całym rynku chińskim. Promowanie solidnej polskiej marki, powinno kojarzyć się Chińczykowi z różnorodnymi i zdrowymi produktami rolno-spożywczymi. Wymaga to jednak konsekwencji i długofalowych działań między innymi poprzez ich prezentowanie na stoiskach narodowych podczas targów organizowanych w Chinach.

EN

After opening of China to the world in 1978, the food market and structure of consumption have changed. The European producers and exporters need to monitor the situation and quickly adapt to the needs of the Chinese consumer. Polish food products are already present at stores in Beijing and Shanghai; they are becoming more recognizable all over China. The Chinese consumers should associate the promotion of the reliable “Polish Brand” with diverse, healthy agri-food products. However, it requires consistency and long-term actions, inter alia by presenting their national stands during the fairs held in China.

2

Nowe dane o minerałach wietrzeniowych złoża Miedzianka-Ciechanowice w Rudawach Janowickich (Dolny Śląsk, Polska)

63%

Siuda R. , Gołębiowska B.

Przegląd Geologiczny

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2011

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tom Vol. 59, nr 3

226-226

EN

The abandoned deposit of polymetallic ore in Miedzianka-Ciechanowice is located in the northern part of the Kowary-Czarnów Unit, within the eastern metamorphic cover of the Karkonosze granite. This deposit is formed mainly of hydrothermal veins related to the Karkonosze granite and Intra-Sudetic Fault. Lenses-forming contact-metasomatic ores are also present. The ore assemblages are rich in Cu, and poor in Pb, Ag, As and Fe. The Miedzianka- -Ciechanowice deposits were mined from the early Middle Ages to the middle of the 20th

3

Primary and secondary copper minerals from Rędziny, Rudawy Janowickie, Sudeten, Southwestern Poland

63%

Orligóra W. , Gołębiowska B.

Geology, Geophysics and Environment

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2012

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tom Vol. 38, no. 4

515--516

EN

Dolomite quarry in Rędziny is a place, which has a very rich polymetallic mineralization. It is a result of hydrothermal processes (precipitated primary minerals) or chemical weathering changes (precipitated secondary minerals). Proximity to Karkonosze Granite massif greatly influenced the variety of the mineralization in Rędziny. Compared to numerous exploited mines located in the vicinity (for example Miedzianka, Ciechanowice, Czarnów, Radomierz), the dolostone quarry is relatively young, opencast mine. Sulfides are the most common primary minerals in Rędziny. This information appears in the study of Gołębiowska et al. (e.g. 1998, 2006, 2012). Secondary mineralization is very variable and it occurs as forms of arsenates, vanadates, phosphates, carbonates, silicates and oxides (Gołębiowska et al. 1998, 2006). The aim of the study was to characterize primary and secondary mineralization, rich in copper compounds, which were located in northern hypergene zone of dolostones quarry in Rędziny. Results were compared with other sampling points from the data of Golebiowska's studies. The chemical analysis in microscale was used to examine relationship between minerals. The presence of Cu-minerals in Rędziny is associated with brownish, greenish and reddish zones dispersed in dolostones. The classic mineralogical and chemical researches of the polymineral samples with macroscopically visible green mineralization with use of optical microscopy (transmitted and reflected light), X-ray powder diffraction (XRD), electron microscopy (SEM) and electron microprobe study (EDS, WDS) were also performed. The main primary minerals are tennantite, chalcopyrite and less often galena or sphalerite. In BSE there were also observed minor mineral inclusions of Ti, U, Ce, Fe and Ca phase, most probably brannerite. It was recognized in small cavities and fissures between relicts of tennanite and it forms prismatic crystals up to 10 |Jin. Origin of brannerite is probably connected with decomposition of uraninite. Minerals of Ti (e.g. titanite) were also found in the Rędziny quarry. The most common secondary mineral phases are represented by Ca-Cu arsenate (tyrolite-clinotyrolite) and Cu-silicate (chrysocolla). X-ray powder difraction data of blue-green spherical accumulation of small crystals, correspond to the standard data of clinotyrolite and partially of tyrolite. Detailed X-Ray studies show split basic reflections: (001) CT and (002) T, and (002) CT and (004) T. These data indicated that tyrolite is intergrowths with clinotyrolite. The analyses of Cu-Ca arsenates were normalized to a X cation =11 (Cu + Ca + Zn + + Fe + Mn + Ba = 11) in the respective formula units of clinotyrolite: Caj 94(Cu8 99, Zn^ 07) [(AsO4)3 95(SO4)0 03 |(OH)10 17] ■ 10H2O. The amounts of H2O were calculated by stoichiometry. Trace elements detected by EMPA are: Mn, Bi, Fe and Ba < 0.01 apfu. Secondary minerals associations from Rędziny quarry were formed differently, which indicate various physical and chemical conditions during oxidation. Supergene phases, which occurs in the northern part of the quarry at Rędziny, were formed as a product of oxidation of primary polymetallic ores, containing sulphides, sulphoarsenides and copper-arsenic sulphosalts.

4

Graftonite-sarcopside intergrowths in phosphate nodulas from pegmatite at Michałkowa, Sowie Mountains Block, SW Poland

51%

Grochowina A. , Gołębiowska B. , Pieczka A.

Geology, Geophysics and Environment

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2012

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tom Vol. 38, no. 4

477--478

EN

Sareopside (Fe,Mn,Mg)3(PO4)2 and graftonite (Fe,Mn,Ca)3(PO4)2 are the dominant minerals found in the phosphate nodules from the Michalkowa pegmatite in the Sowie Mountains block. The nodules are rather small with mainly varying brown coloration and with lamellar texture visible in hand specimen. Both minerals occur with other primary and secondary phosphates in the form of nodules like triphylite or ferrisicklerite, stanekite or wolfeite, members of the arrojadite and wyllieite groups, kryzhanovskite, fluorapatite and others. Apart of typical pegmatite minerals like quartz, microcline, albite, muscovite and biotite, only black tourmaline can be found. Pyrrhotite, pyrite and chalcopyrite, occurring in the form of tiny grains or veinlets, penetrating also the phosphate nodules are common. Standard mineralogical investigations (light and reflected microscopy, XRD), combined with SEM-EDS analyses and WDS method were carried out to characterize these phases. Graftonite and sareopside form massive aggregates of euhedral crystals or lamellar intergrowths. Euhedral crystals of sareopside are typically enriched in Mn and Mg. Ca is commonly absent or present in negligible amounts. MnO usually ranges between 10.0-11.0 wt. %; only locally reaches a higher content up to 13.3 wt. %, MgO content commonly reaching 4.0-5.0 wt. %, or only about 2.0 wt. % in Mn-rich compositions. The lamellar sareopside shows compositional characteristics similar to the variety forming the euhedral crystals. In consequence, the Mn/(Mn+Fe) ratio that informs about a degree of Mn-Fe fractionation in the parental, pegmatite forming melt, attains in both morphological varieties of sareopside rather low values, usually 0.18-0.20. In graftonite the CaO content is higher in crystals co-occurring with euhedral sareopside, reaching in this variety up to 11.0 wt. %, whereas the lamellar graftonite has only 6-7 wt. % of the component. In both types of graftonite the contents of MgO are less than in sarcopsi-de and they do not exceed 2.0 wt. %. Graftonite richer in Ca is simultaneously poorer in Mg. FeO content is higher in graftonite forming lammelar intergrowths with sarcopside (31.0-32.0 wt. %), and slightly lower in euhedral crystals (27.0-28.0 wt. %). Manganese is close similar in both varieties, whereas Zn is undetectable or present in a small content distinctly below 1 wt. % ZnO. The lower Mn/(Mn+Fe) values (0.36-0.39) are characteristic of lamellar graftonite; only slightly higher values (0.40-0.41) attains graftonite in association with euhedral sarcopside. Both minerals show weakly varying compositions resulted from homovalent substitutions (Fe, Mn)2+ <-> Mg2+ and Ca2+ <-> (Fe, Mn)2+ marked in varying values of Mn/(Mn+Fe) ratio. The minerals crystallized from the parental P-bearing melt exsolved from pegmatite-forming silica melt during temperature decreasing. The formation of the massive or lamellar forms depends on a relationship between amounts of the exsolved Ca-and P-bearing melt and its Ca-negligible counterpart.

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Manganese oxides from Zalas, Kraków area, southern Poland

51%

Polak M. , Gołębiowska B. , Rzepa G.

Geology, Geophysics and Environment

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2016

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tom Vol. 42, no. 1

120--121

EN

The Zalas quarry is located in the southern, marginal part of the Silesian-Cracovian Monocline. Permian rhyodacite laccolith has been exploited here for over 70 years. The intrusion was formed about 260–280 Ma during the Early Permian transtensional, sinistral tectonic regime predominating in central Europe at that time (Nawrocki et al. 2005). Permian volcanic rocks are overlain by a Middle–Upper Jurassic sedimentary sequence, built from sands and sandstones, substituted with the passing of time by limestones and sandy limestones rich in fossils (Matyszkiewicz et al. 2006). Quarrying operations carried out approximately 10 years ago uncovered a fault zone cutting the Middle Jurassic sandy limestones. Exposed breccias was locally encrusted by a hydrothermal mineralization forming thin veinlets cutting the limestone, or surrounding the breccia clasts. Primary mineralization contained small relics of pyrite, chalcopyrite, chalcocite, galena, native bismuth and barite and was significantly replaced by supergene minerals e.g. Fe and Mn oxides, malachite, cuprite, Cu sulphates, iodargyrite, Bi oxychlorides and Na, K chlorides (Gołębiowska et al. 2006, 2010, 2015). The mineralization is most likely connected with rejuvenation of Early-Paleozoic fault zones during the Sava phase of the Alpine orogeny, and subsequent intensive weathering under semi-arid and arid climate in a period between the Oligocene and Middle Miocene (Gołębiowska et al. 2010). In the sandy limestone encrusted by the oxidized mineralization, very interesting Mn-oxides, enriched in numerous heavy metals were encountered. They filled small fractures and voids within the fault breccia. Among them, Tl-rich varieties have been recently reported. Extremely high thallium content, reaching 20.82 wt% Tl 2 O, makes the oxides unique on a world scale (Gołębiowska et al. 2015). In this paper we focused on the variable admixtures in Mn oxides from oxidation zone in Zalas; for this purpose, SEM-EDS and WDS analyses were carried out. Mn oxides in Zalas are accompanied by malachite, Fe oxides (goethite and hematite) and relics of primary mineralization (Matyszkiewicz et al. 2015). Mn and Fe oxides commonly form the yellowish to red-brownish or black tiny grains or cryptocrystalline aggregates with sizes up to a few millimetres across. Manganese oxides contain variable admixtures of Cu, Ca, Pb, Ba, Fe, Ni, Co and Tl. On the basis of chemical analyses, three major Mn oxide types have been distinguished: those enriched in (i) Ni and Co, (ii) Pb and (iii) Ba and Ca. Co-Ni-bearing Mn oxides, probably asbolane-type, contain 17.01–21.58 wt% CoO and 3.05–8.33 wt% NiO. These phases contain also admixtures of Cu (up to 10 wt% CuO) and Al (up to 7 wt% of Al 2 O 3 ), as well as traces of Fe, Ba, Zn, Mg and Tl (up to 0.5 wt%). Interestingly, in Mn oxides of this type, the admixtures of lead are absent. Pb-bearing Mn oxide, probably coronadite, contain up to 21.48 wt% PbO. In its composition various other elements were also noticed: up to 2 wt% CoO, 0.4 wt% NiO and very high concentrations of CuO up to 8 wt%, as well as up to 1 wt% BaO, FeO, CaO Tl 2 O, Al 2 O 3 and traces of Zn and Mg. Chemical mapping indicates that the Ba- or Ca-bearing Mn oxides occur only in marginal parts of zoned MnO 2 aggregates with almost pure MnO 2 in their cores. They contain 78–84 wt% MnO 2, 3–10 wt% BaO and 2.5–4.5 wt% CaO. High contents of Co, Ni, Pb, Cu and Tl in Mn oxides from Zalas indicate a direct link with the primary ore assemblage. High concentration of cobalt and nickel might suggest some connection with Co and Ni mineralization known from nearby Karniowice Travertine (Czerny 1992). Mineral association, as well as crystal morphologies and sizes could indicate hydrothermal origin of at least part of the Mn oxides. However, identification of the particular minerals as well as concluding on the details of their origin is quite difficult on this stage of research.

6

Polymetamorphic evolution of pelites inferred from tourmaline zoning – the Rędziny hornfels case study at the eastern contact of the Karkonosze Granite, Sudetes, Poland

45%

Majka J. , Sęk M. P. , Mazur S. , Gołębiowska B. , Pieczka A.

Mineralogia

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2018

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tom Vol. 49, iss. 1/4

17--34

EN

Tourmaline occurring in hornfelses from the eastern envelope of the Karkonosze Granite (Western Sudetes, Poland) reveals at least two stages of crystallization expressed by its complex zoning. The cores and mantles of the crystals probably grew during prograde metamorphism under intermediate pressure-temperature conditions reflected by increasing Mg, Ti and Ca. Outermost rims show enrichment in Al and Ca, indicating growth during contact metamorphism in the presence of an Al-saturating phase. The Ti-content in biotite indicates that the temperature of the contact metamorphic event did not exceed 650ºC. The presence of andalusite and the lack of garnet and cordierite also indicates pressure conditions of ~ 2-3 kbar, typical of the C1 bathozone of Carmichael (1978) or the P1 bathozone of Pattison (2001).

7

The philipsbornite–segnitite solid-solution series from Rędziny, eastern metamorphic cover of the Karkonosze granite (SW Poland)

45%

Gołębiowska B. , Włodek A. , Pieczka A. , Borkiewicz O. , Polak M.

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tom Vol. 86, No. 1

73--83

EN

Supergene minerals of the philipsbornite–segnitite series, PbAl3(AsO4)(AsO3OH)(OH)6–PbFe3+3(AsO4) (AsO3OH)(OH)6, accompanied by carminite, PbFe3+2(AsO4)2(OH)2, were found in relics of hydrothermal quartz– chlorite–arsenopyrite veins, associated with subordinate polymetallic ores disseminated in contact zones of a dolomitic marble deposit at Rędziny, Western Sudetes, Poland, and recognized by means of electron microprobe and X-ray and electron-back-scattered diffraction (XRD and EBSD). Philipsbornite and segnitite, as the two minerals of the series, exhibit highly variable compositions, especially in terms of the range of Fe3+ Al3+ substitution at the G site, with a distinct gap between the values of 0.52 and 0.89 for the Fe/(Al+Fe) ratio; substitutions at the D and T sites are less important. In this respect, the minerals are almost identical with philipsbornite and segnitite, known from other localities. The gap might be a consequence of the limited miscibility of the end-members, but also might be attributed to crystallization under the changing and distinctly differing activities of Al3+ and Fe3+. The unit-cell parameters of philipsbornite, a = 7.1245(13) Ο, c = 17.0967(45) Ο, make the mineral comparable with philipsbornites from other occurrences. The EBSD analysis confirmed the rhombohedral structure of both minerals and the space group symmetry R-3m. The minerals crystallized in the sequence: philipsbornite -> segnitite -> carminite, which reflects (i) decreasing acidity in the oxidation zone, due to the leaching of sulphate ions and interaction of the solutions with a nearby dolomite lens, and (ii) varying activities of Al3+, Fe3+ and Pb2+ cations, mobilized by the solutions through interaction with the silicate host containing disseminated arsenopyrite and subordinate sulphides, up to complete Pb2+ depletion.

8

Epigenetic silicification of the Upper Oxfordian limestones in the Sokole Hills (Kraków-Częstochowa Upland): relationship to facies development and tectonics

38%

Matyszkiewicz J. , Kochman A. , Rzepa G. , Gołębiowska B. , Krajewski M. , Gaidzik K. , Żaba J.

Acta Geologica Polonica

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2015

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tom Vol. 65, no. 2

181--203

EN

A spectacular epigenetic silicification was encountered in the Oxfordian bedded limestones exposed in the Sokole Hills situated in the Kraków-Częstochowa Upland. The main epigenetic mineral is microcrystalline quartz accompanied by minor goethite, hematite, barite, galena and sphalerite. Locally, the mineralized limestones reveal Pb and Cu contents exceeding over 150 times the background values of these metals in unmineralized limestones. The epigenetic mineralization of the bedded limestones was probably a two-stage process. During the first, Early Cretaceous stage, silicified limestones formed at the erosional surface of a denuded carbonate complex. Such silicification greatly limited the progress of the first karstification phase of the Upper Jurassic carbonates initiated in the Hauterivian. The sources of silica accumulated in the limestones were descending solutions enriched in silica derived from the weathering zone. This silicification affected the topmost part of the Upper Jurassic massive limestones and the deeper portions of the bedded limestones along the fracture systems and stylolites. Early Cretaceous tectonic activity generated new dislocations and re-opened the existing faults, which were subsequently filled with permeable Albian quartz sands. These openings became the migration pathways for ascending, warm, relict, sulphide-carrying hydrothermal solutions at the second formation stage of the epigenetic mineralization. The newly supplied silica from the Albian sands precipitated on the silicified limestones and, as concentric rims, on brecciated, early diagenetic cherts. The second-stage mineralization proceeded under phreatic conditions, presumably close to a fluctuating mixing zone of ascending, warm hydrothermal solutions and descending cold groundwaters. The brecciated cherts acting as silica crystallization nuclei indicate that the last mineralization stage probably followed the final phase of Cenozoic faulting.