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Experimental Investigation on the Load Signature Parameters for Non-Intrusive Load Monitoring

Bacurau R., Dante A., Duarte L., Ferreira E.

Przegląd Elektrotechniczny

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2015

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R. 91, nr 8

86--90

PL

W artykule zaprezentowano eksperymentalne studium w którym zmierzono parametry typowych urządzeń elektrycznych w celu określenia i zestawienia obciążeń. Stwierdzono że moc czynna, moc bierna, napięcie skuteczne i pierwsze pięć nieparzystych harmonicznych prądu mogą stanowić podstawę do prognozowania obciążeń.

EN

One of the most important design decisions in Non-Intrusive Load Monitoring (NILM) systems is choosing which electrical parameters will be used to define load signatures. In this paper, we present an experimental study where several electrical quantities of common home appliances were measured, in order to identify the most adequate to perform load disaggregation. It was found that active power, reactive power, rms voltage, and the first five odd harmonics of the current and voltage signals comprises the best set of parameters to define the signatures of residential loads.

2

Sequence stratigraphy and depositional setting of the Pliensbachian and Toarcian marly limestones in the Lusitanian Basin, Portugal

Duarte L.

Volumina Jurassica

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2006

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Vol. 4, no. 1

157-158

EN

The Pliensbachian and Toarcian series in the Lusitanian Basin (Portugal) are generally dominated by hemipelagic deposits, represented by marl/limestone alternations that are very rich in nektonic and benthic fauna. These sediments are included in the following four formations: Vale das Fontes, Lemede, S. Giăo and, partially, Póvoa da Lomba. The weak lateral facies variation, generally observed at the basin scale, suggests that these sediments were deposited in an epicontinental extensional basin on a homoclinal carbonate ramp controlled by eustatic fluctuations and regional tectonics. Considering the Late Triassic – Late Callovian large cycle, the sediments correspond to the maximum transgressive facies which can be widely observed throughout the succession. A detailed studied of several stratigraphic sections in terms of sedimentological, geochemical and paleontological analysis shows that the Pliensbachian-Toarcian series is subdivided into two second-order sequences (SP and ST). The Pliensbachian succession shows a typical second-order transgressive/regressive sequence, with a dominant marly deposition at the base and a calcareous dominant facies at the top. The basal discontinuity of the SP is particularly well observed in the western part of the basin, dating roughly from the Sinemurian/Pliensbachian boundary. The series shows a large transgressive phase, ending in the middle-upper part of the Margaritatus Zone (around Subnodosus/Gibbosus subzones boundary) associated with an organic-rich deposition verified at the basin scale. During the Spinatum Zone the sedimentation returned to a calcareous regime very rich in benthic macrofauna. The upper discontinuity of the SP observed in the whole basin dates from the lowermost Polymorphum Zone (intra-Mirable Subzone). The base of ST (Polymorphum Zone) corresponds to an abrupt flooding event, through a generalised marly accumulation in the whole basin. However, around the Polymorphum-Levisoni interval, an important tectonic activity occurred, responsible for a great sedimentary change with special facies features in some positions of the basin. The dominance of marl observed at the top of the Levisoni Zone marks the maximum peak transgression of the Toarcian second-order sequence, showing some evidence of pelagic deposition, with thin-shelled bivalve-rich (Bositra sp.) horizons. The Upper Toarcian – Lower Aalenian succession shows a regressive trend, ending ST with an upward increase of calcareous and bioclastic content, including ahermatipic corals in the eastern sectors. The upper discontinuity dates from the Opalinum Zone and shows different sedimentary records across the basin. ST it is subdivided into four third-order depositional sequences (St1 to St4), each bounded by regional discontinuities, recognized over most parts of the Lusitanian Basin.

3

Recent data on the ostracod fauna from the Lower and Middle Toarcian of Peniche, Portugal

Pinto S., Cabral M., Duarte L.

Volumina Jurassica

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2006

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Vol. 4, no. 1

204-205

EN

At Peniche region, western Portugal, a rather continuous marly limestone succession ranging in age from the Sinemurian to the earliest Aalenian crops out. The ostracod fauna from a 74 m thick packet within this succession has been studied, encompassing deposits that range from the topmost Pliensbachian (topmost Spinatum Biozone) to the Middle Toarcian (Polymorphum, Levisoni, Bifrons and basal Gradata biozones). The studied levels belong to Lemede (2 m) and Cabo Carvoeiro Formations. From the 47 samples collected in the marly layers, a single one is azoic. Sample numbers and bed subdivision are according to biozonation in Duarte (1995), which considers 5 packets: topmost Spinatum, Polymorphum, Levisoni, Levisoni+Bifrons, Bifrons+basal Gradata. The systematic study of the ostracods has been undertaken, and some palaeoecological aspects have also been addressed, namely hydrodynamics (carapace/valve ratio), bathymetry and oxygenation, based on marker genera/groups. Around 8000 individuals were obtained (1 individual =1 carapace or 1 valve), which are commonly badly preserved. At least 58 species belonging to 22 genera have been identified until now. The top of Spinatum Biozone displays both high diversity (8-15 species/sample) and abundance (222-402 individuals/sample) of ostracods. The dominant species are from the genus Ogmoconcha, Ogmoconchella and Liasina, associated with Polycope, Paracypris, Ledahia, among others. The Polymorphum Biozone shows high diversity (3-22 species/sample) and variable abundance (1-150 individuals/sample). The genera Ogmoconcha, Ogmoconchella and Liasina still dominate and, from the first levels of the biozone, heavily ornamented species of Kinkelinella are present; the genus Isobythocypris occurs for the first time. In Levisoni Biozone, the ostracod diversity (1-4 species/sample) and abundance (1-150 individuals/ sample) are low, in contrast with previous biozones. Ogmoconcha and Ogmoconchella disappear, and the genus Cytherella appears for the first time, becoming dominant together with Liasina in the first levels of the biozone. In the upper part, Kinkelinella dominates and at the top Bairdiacypris and Cytheroptheron occur for the first time. Levisoni+Bifrons shows that ostracod diversity is moderate (5-11 species/sample) and abundance is high (60-310 individuals/sample). Species from the genera Bairdiacypris and Kinkelinella dominate, Cytherella and Patellacythere are common. Bifrons+basal Gradata shows higher diversity (3-18 species/sample) than previous unit and variable abundance (16-468 individuals/sample). Bairdiacypris, Cytherella and Kinkelinella dominate, and Macrocypris and Trachycythere(?) occur for the first time. All of the recognized species have been found in formations of a similar age in Western Europe, and are benthic marine species, except the genus Polycope (pelagic). Most of the species indicates a deep marine setting, with variable oxygenation levels, from normal to low (predominance of Metacopina and Cytherella), for the all section. The water energy was also variable, being stronger at the topmost Spinatum and Polymorphum biozones, within which ostracod valves are dominant, and lower at the Levisoni and Levisoni+Bifrons biozones, within which ostracod carapaces clearly dominate.

4

Pliensbachian – lowermost Toarcian chemostratigraphy (elemental and TOC) of the Peniche section (Lusitanian Basin, Portugal)

Veiga de Oliveira L., Duarte L., Rodrigues R.

Volumina Jurassica

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2006

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Vol. 4, no. 1

217-218

EN

In Portugal, the Peniche section constitutes one of the most continuous series of Lower Jurassic. This study is based on a detailed chemostratigraphic analysis of the Pliensbachian - lowermost Toarcian marly limestones, belonging to the Vale das Fontes, Lemede and Cabo Carvoeiro formations. 196 samples of limestones and marls were analyzed in terms of minor and major elements (Fig. 1). Total organic carbon (TOC) was determined in 233 samples. Besides the stratigraphic distribution of these geochemical parameters, the aim of this work is to perform a discussion about biogenic influx and aluminosilicate phasefluxes. The Al concentrations are a good indicator of detrital flux and good correlations between them signify aluminosilicate affiliation. In Peniche, K (0.98), Si (0.96) and Ti (0.98) show, in all section, excellent correlation with Al2O3. Mg (0.82), Ba (0.80), Cr (0.78), Li (0.80), Na (0.74), Sc (0.80), V (0.81) and Zr (0.86) correlate well with Al2O3 but other secondary factors, beyond the detrital flux, affect the resultant concentrations. The Pearson's coefficients between Al2O3 and CaO is strongly negative (-0.98), suggesting divergent behaviours for this elements. Al2O3 and Fe2O3 correlate moderately (0.61). However, the correlation coefficients calculated for each stratigraphic unit show variable values. Lemede Formation and the Members Marls and Limestones with Uptonia and Pentacrinus (MLUP), Lumpy Marls and Limestones (LML), to the Vale das Fontes Formation, and CC1, to the Cabo Carvoeiro Formation, show high correlation coefficients between Al2O3 and Fe2O3 (0.87, 0.91, 0.88 and 0.97, respectively). On the other hand, the Member CC2 has moderate correlation (0.67) and the Member Marls and Limestones with Bituminous Shales (MLBF) has weak correlation (0.20). These variations suggest that the elemental inputs change during the Pliensbachian - lowermost Toarcian, in the Peniche area. Ba enrichment is considered an indicator of high flux of biogenic material and high surface-water productivity. But, in the studied section, correlation between Al2O3 and Ba is high (0.80) and Ba lacks any correlation with TOC (0.17). Thus, in the Peniche region, the distribution of Ba is dominated by the original detrital flux and transported to the basin, mainly, as a constituent of clays. The mainly TOC values in the Pliensbachian - lowermost Toarcian of the Peniche section are below 2. But the MLBF (Ibex to Margaritatus zones) represents a high TOC interval with concentrations up to 15%, correlated with the 2nd order flooding interval, well know in the Lusitanian Basin.

5

Pliensbachian calcareous nannofossil zones vs ammonite zones along the western and northern margins of the Iberian Massif and biostratigraphical potential of nannobiohorizons

Perilli N., Veiga de Oliveira L., Comas-Rengifo M., Duarte L.

Volumina Jurassica

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2006

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Vol. 4, no. 1

202-203

EN

Calcareous nannofossils, one of the main components of Lower Jurassic marly/limestone alternations, were studied along the western and northern margins of the Iberian Massif. Consequently, they were used to date the lithological successions as well abiotic signals (e.g. isotope or TOC profiles). Our work focuses on the main changes of calcareous nannofossil record and the biohorizons recognized in some reference Pliensbachian sections from Basque-Cantabrian area (Spain) and Lusitanian Basin (Portugal). The remarkable changes in composition are the appearances and abundance increases of the Biscutaceae (Similiscutum) and of Watznaueriaceae (Lotharingius). The appearances of large Biscutum (B. grande and B. finchii) and of medium-sized Lotharingius species (L. sigillatus) are also clearly detectable though their occurrence is discontinuous. The other events include the appearances of Biscutum dubium, Bussonius prinsii, Biscutum novum and Crepidolithus impontus and the disappearance of Parhabdolithus robustus. The reconstructed distribution pattern of the age-significant species supports the identification and description of the nannofossil zones and subzones proposed for NW Europe. The NJ3/NJ4, NJ4/NJ5 zone boundaries are easily identified by the FO of Similiscutum cruciulus (Lower Pliensbachian) and the FO of Lotharingius hauffii (Upper Pliensbachian), respectively. The subzone boundaries should be carefully checked because the zonal markers are rare and occur discontinuously. However, the other events are helpful to correlate the biostratigraphic frames outlined for the investigated areas and to calibrate the NJ4a/NJ4b, NJ5a/NJ5b zone boundaries with respect to the ammonite zones. Based on the achieved data, the main differences between the two schemes are related to the very low abundance and discontinuous occurrence of the some species in their initial (e.g., B. grande, B. finchii) or final (e.g., P. robustus) ranges. Since for the Basque-Cantabrian area ammonite zone and subzones are well constrained, some discrepancies should be related with a discontinuous or incomplete ammonite record from the Lusitanian Basin. Nevertheless, the biostratigraphic frames proposed for both areas could improve biochronocorrelation between the Pliensbachian successions cropping out along the western and northern margin of the Iberian Massif.

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Microbial mounds from the restricted-marine Sinemurian succession of S. Pedro de Moel (Lusitanian Basin, Portugal): preliminary palaeoecological interpretation

Azeredo A., Duarte L., Cabral M.

Volumina Jurassica

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2006

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Vol. 4, no. 1

77-77

EN

In the Lusitanian Basin the Sinemurian corresponds to a marginal- to restricted-marine succession, representing the early stage of sea flooding in the recently formed basin, following a Late Triassic rifting event. Except for its topmost part, the Sinemurian succession belongs to the Coimbra Fm., composed of dolostones, dolomitic limestones and limestones. This unit is dominated by peritidal facies towards the eastern, more landward zone of the basin, whereas in the W (as at S. Pedro de Moel) more distal (though not quite deep) facies occur. At S. Pedro de Moel the Coimbra Fm. is well exposed and the section displays a succession mostly composed of argillaceous and/or dolomitic limestones and fossiliferous/skeletal limestones (bivalves, gastropods, ostracods), interbedded with a few marly levels. Although fossil remains are commonly present in variable amounts, some beds seem to be azoic, others exhibit rare, deformed burrows and very rare ostracods. Undulating, irregularly bounded, laminar levels are common and, locally, centimetre to decimetre-thick concentrated skeletal/fossil layers occur. However, towards the middle part of the section, well-preserved, dome-shaped stromatolites occur, in clear contrast with the under- and overlying bedded deposits. Towards the top of the succession, the calcareous/clay ratio increases. This section is still under study, so we only make a preliminary palaeoenvironmental approach here. The microbial mounds have an average maximal thickness of 0.75 m and show different fabrics, sometimes within the same mound: laminated, stromatolitic crusts; clotted, peloidal micrite; micritic and sparitic threads; degraded, tuft-like filamentous structures; enhanced fenestral-like porosity; dense, slightly darker micrite. These features suggest that they were formed through hardening of calcified cyanobacterial and other microbial films, whose early disintegration also would have contributed with autochthonous mud for the mounds. However, a more detailed study is clearly needed. It is known from the literature that microbialites, as a whole, may form in a wide range of environmental conditions, though some associations or particular morphologies may give us more accurate ecological information. However, a crucial basic condition is a very low to low background sedimentation. In the present case, it is suggested that the stromatolites grew under low-energy, restricted water-circulation and low rate of mixed terrigenous and calcareous mud deposition. A likely nutrient-poor substrate, the existence of terrigenous material and, maybe, slight (?)hypersalinity would have inhibited a more significant development of epibenthic and heterotrophic organisms, favouring the microbial community. The low energy prevented physical erosion which, coupled with the absence of predators, allowed the development of the well-defined dome morphologies. In contrast, towards the top of the succession a more open setting prevailed, with better water-circulation, probably better oxygenation and somewhat higher sedimentation rate with dramatic decrease of clay material. Though most of the upper deposits are still low-energy ones (biomicrite mudstones and wackestones, with a few ostracods, gastropods, bivalves, rare hyaline forams), skeletal/intraclastic/peloidal packstones and rarer grainstones occur more frequently, attesting for the less protected environment. These conditions did not allow the continuation of microbial growth.

7

Calcareous nannofossils biostratigraphy and oxygen isotope composition of belemnites: Pliensbachian – lowermost Toarcian of Peniche (Lusitanian Basin, Portugal)

Veiga de Oliveira L., Duarte L., Rodrigues R., Perilli N.

Volumina Jurassica

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2006

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Vol. 4, no. 1

219-219

EN

The Lusitanian Basin is located in the western Iberian margin, opened during the Triassic.The Lower Jurassic is particularly well represented at Peniche, which exhibits a continuous seriesof carbonate sediments, more than 450 m thick and aged between Sinemurian and Toarcian.In lithostratigraphic terms it corresponds to the Agua de Madeiros, Vale das Fontes, Lemede and CaboCarvoeiro formations. In this study, 145 m thick section (from the Jamesoni to the Levisoni ammonite zones),was analyzed in terms of calcareous nannofossils biostratigraphy and oxygen isotopes of belemnite rostra.The nannofossil biozones NJ4a, NJ4b, NJ5a (Pliensbachian; upper part of Jamesoni to Spinatumammonite zones), NJ5b (uppermost Pliensbachian - lowermost Toarcian; upper part of Spinatumto Levisoni ammonite zones) and NJ6 (lowermost Toarcian; upper part of Levisoni ammonite Zone) wereidentified based on proposed NW European schema and correlated with ammonite zones. Additionally,the secondary biostratigraphic events were registered which will be useful to refine the nannofossilsbiozonation: the first occurrences (FO) of Biscutum grande and B. finchii were found in the upper part ofthe NJ4a biozone (lower part of Margaritatus ammonite Zone); the FO of Lotharingius frodoi wasidentified at the same stratigraphical level as L. hauffii; the FO of L. sigillatus was found in the upper partof the NJ5a biozone (Spinatum Zone); the first common occurrence (FCO) of Calyculus spp. was recognizedin the NJ5b base, near the Pliensbachian/Toarcian boundary; the FO of Carinolithus spp. was identifiedwithin NJ5b biozone, correlated with the lower part of the Levisoni ammonite Zone and below the extinctionlevels of Calcivascularis jansae and B. grande which are other nannofossil secondary events.The oxygen-isotope profile of the Peniche section seems to reflect primary signals and can be usedto interpret the sea water paleotemperatures variations. In the Early Pliensbachian the temperature showsa gradual cooling trend (NJ3 and the lower part of the NJ4a; Jamesoni ammonite Zone). Afterward,there is a warm period (NJ4a and NJ4b; Jamesoni to lower part of Spinatum ammonite Zone) correlatedwith high TOC values interval (up to 15%), suggesting a relative sea level rise and concomitant high surfacewaterproductivity. In fact, the Margaritatus ammonite Zone corresponds, in the Lusitanian Basin,to 2nd-order flooding interval. In the Late Pliensbachian and Early Toarcian (NJ5a and lowermost partof NJ5b; Spinatum to Polymorphum ammonite zones), the isotopic values show slight variations.However, they suggest a small cooling trend in the upper part of Spinatum ammonite Zone and a warmtendency in the lower part of Polymorphum ammonite Zone.

8

Apparent sea-level change at times of extraordinary sediment supply: integrated facies analysis and chemostratigraphy of Early Toarcian Oceanic Anoxic Event, Peniche, Portugal

Hesselbo S., Jenkyns H., Duarte L., Veiga de Oliviera L.

Volumina Jurassica

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2006

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Vol. 4, no. 1

171-172

EN

The Toarcian Oceanic Anoxic Event in the Early Jurassic was a time of major environmental change characterized by widespread deposition of organic-rich black shales in both deep- and shallow-marine settings. Facies evidence, mainly from the European area, has been used to argue for a major sea-level rise in concert with oceanic anoxia, extinction of certain groups, and perturbation of the carbon cycle. However, in a number of locations, such as in the Lusitanian Basin, Portugal, it has also been argued previously that the start of the event was characterized by sea-level fall rather than rise, as evidenced by the initiation of gravity-flow deposition. In this study we combine new marine and terrestrial carbon-isotope and lithological data to suggest an alternative model for development of facies patterns in this basin, whereby an abrupt increase in sediment flux from the hinterland led to slope instability and gravity-flow deposition that lasted as long as the carbon-cycle perturbation. This interpretation is supported by existing osmium and strontium isotope data, which have been interpreted to indicate a significant continental transient increase in continental weathering fluxes. In effect this event provides a good example from the rock record where the assumption of constant sediment supply is demonstrably false, but in which the facies patterns may still be predictable on a variety of scales.

9

Ammonites from Lias-Dogger of n’Zala (Central High Atlas, Morocco)

El Hariri K., Henriques M., Chafiki D., Duarte L., Ibouh H.

Volumina Jurassica

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2006

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Vol. 4, no. 1

170-171

EN

This work aims at presenting the n’Zala section as a reference section characterizing the Lias/Dogger interval in the Moroccan Central High Atlas, both from the biostratigraphic point of view and the knowledge of some Ammonitina associations (recorded there). The n’Zala section is situated on the northern side of Jbel Aouja, near n’Zala Village, about thirty kilometers north of the village at the main road n° 21. The marly-limestone succession partly corresponds to the lower part of the Agoudim Formation. The studied interval covers about 60 metres and its major part consists of decimetric to metric thick alternation of micritic limestones and fissile marls. A study of 250 specimens belonging to over 30 taxa of Ammonitina, Lytoceratina and Phylloceratina makes it possible to recognize biostratigraphic units characterizing the Lias-Dogger interval at n’Zala, particularly the Meneghini Biozone (top), the Aalensis Biozone, the Opalinum Biozone (Opalinum and Comptum subzones) and the base of Murchisonae Biozone (Haugi Subzone). The Meneghini Biozone (about 15 m thick) at the base of the section is characterized by abundance of Catulloceras sp. associated with some Vacekia sp. and some Cotteswoldia sp. One can also notice the presence of Hammatoceratinae (particularly notable Hammatoceras aff insigne) associated with Lytoceratina and Phylloceratina. At the base of the Aalensis Biozone (about 12 m thick), we did not record Pleydellia mactra, the species index of the Mactra Biozone, but an abundance of Tmetoceras scissum, associated with Vacekia sp. along with Lytoceratina and P. aalensis, which appear in the lowest levels of the zone. Below, we found representatives of the species index of the Aalensis Subzone, Pleydellia aalensis, associated with Tmetoceras scissum and Vacekia sp. but without P. mactra. Note that Lytoceratina and Phylloceratina are also present there. The base of the Opalinum Biozone is characterized by the first appearance of forms belonging to the Cypholioceras – Leioceras dimorphic couple. The Opalinum Subzone (about 10 m thick) is defined by striated forms of Cypholioceras sp. along with Leioceras sp., Vacekia sp., Phylloceratina and Lytoceratina. The base of the Comptum Subzone (about 8 m thick) is marked by the presence of the costated representatives of Leioceras (Leioceras cf. comptum, Leioceras costusum), which are associated with Tmetoceras (Tmetoceras scissum and Tmetoceras sp.) along with Planammatoceras, Hammatoceras and Lytoceratina. The base of Murchisonae Biozone is defined by the first appearance of Graphoceratidae (Ancolioceras opalinoides, Ludwigia aff. haugi) characterizing the Haugi Subzone (about 30 m thick). The Tmetoceras sp. and Vacekia sp. persist in the biozone along with the Hammatoceratidae, the Phylloceratina and Lytoceratina. In the n’Zala section, the ammonite associations of the Lias-Dogger interval show marked biostratigraphic and paleogeographic changes. In the Aalensis Biozone, the ammonite associations show a clear Tethyan affinities as indicated by common occurrence of taxa belonging to Hammatocerataceae, Lytoceratina and Phylloceratina. The Opalinum and Murchisonae biozones show rather NW European influences, with a predominance of representatives of Leioceratinae and Graphoceratina consequently allowing the recognition of biostratigraphic units at the level of the subzones.