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Acquisition of databases for facial analysis

Malawski F.

Challenges of Modern Technology

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2016

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Vol. 7, no. 3

3--7

EN

This article describes guidelines and recommendations for acquisition of databases for facial analysis. New devices and methods for both face recognition and facial expression recognition are constantly developed. In order to evaluate these devices and methods, dedicated datasets are recorded. Acquisition of a database for facial analysis is not an easy task and requires taking into account multiple issues. Based on our experience with recording databases for facial expression recognition, we provide guidelines regarding the acquisition process. Multiple aspects of such process are discussed in this work, namely selection of sensors and data streams, design and structure of the database, technical aspects, acquisition conditions and design of the user interface. Recommendations how to address these aspects are provided and justified. An acquisition software, designed according to these guidelines, is also discussed. The software was used for recording an extended version of our previous facial expression recognition database and proved to both ensure correct data and be convenient for the recorded subjects.

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Sedimentary record of the Dukla Basin (Outer Carpathians, Slovakia and Poland) and its implications for basin evolution

Dirnerová D., Prekopová M., Janočko J.

Geological Quarterly

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2012

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Vol. 56, No 3

547--560

EN

The Late Cretaceous to Oligocene strata of the Dukla Nappe, which is a part of the accretionary wedge formed in front of the Carpathian orogen, record a history of the basin development from remnant to foreland basin stages. The lower part of the succession indicates the first stage of basin evolution characterized by turbidite systems fed from the E (NE) to W (SW). The system encompasses deposits of the Łupków and Cisna formations deposited in a channel-lobe transition (Łupków Fm.) and in sandstone-rich channelized lobes (Cisna Fm.) The transitional phase is represented by deposits of the Submenilite Formation derived from two different sources (SE and N) and deposited in a submarine slope/ramp environment. The third stage of basin evolution is marked by the advancing front of the Carpathian orogen resulting in peripheral foreland basin development. Increased tectonic activity led to a switch in sediment source from the SE to the NW, more complex topography of the basin and a change in sediment distribution. The initial phase of this stage is characterized by low-density turbidites and suspension fall-out sediments of the Menilite Fm. Discrete tectonic pulses are recorded by the thick Cergowa sandstones, mostly deposited by hybrid flows and high-density turbidity currents. A decrease in tectonic activity is suggested by heterolithic deposits of the Krosno Fm. capping the sedimentary succession.

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Osady deglacjacyjne zlodowacenia Warty we wschodniej części regionu łódzkiego

Rdzany Z.

Przegląd Geologiczny

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2006

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Vol. 54, nr 4

343-351

EN

The author attempts at formulating a synthetic description of geological and geomorphological effects of theWartanian ice-sheet deglaciation in the eastern part of the Łódź region, taking their spatial variability into consideration. Characteristic features of Wartanian Glaciation sediments occur in this area, and their lithofacial diversity and spatial distribution needed interpretation. The deposits document the complex processes of deglaciation, which developed here across an unusually broad area in the scale of the Polish Lowland. The best developed deglaciation sediments occur in the eastern part of the Łódź Heights, between the Mroga and Rawka rivers, as structural components of different types of kames and glaciofluvial covers. In locations where glacial till is elevated they include mainly sediments of braided rivers and alluvial cones, whereas in areas of wide depressions of till and, thus, of the ice-sheet bedrock — glaciolimnic sediments prevail. The highest and most diverse western part of the Łódź Heights is characterised by the occurrence of thin and discontinuous deglaciation sediments, because this area was shaped mainly during the ice-sheet transgression. During deglaciation, ablation waters left mainly traces of erosion, whereas the glaciofluvial accumulation series are not well developed. In the Rawa Interfluve, deglaciation sediments accumulated predominantly at the early deglaciation stage in sparesely distributed broad basins of kame sedimentation. In the Piotrków Plain, deglaciation deposits are thin; ice-sheet disintegration proceeded without major blockages of ablation waters, resulting in a less diverse interfluvial landscape.