Wind-Battery-PV Based Microgrid with Discrete Second Order Sequence Filter-Frequency Locked Loop

2020 ◽  
Author(s):  
Sudip Bhattacharyya ◽  
Bhim Singh
Keyword(s):  
Second Order ◽  
Order Sequence ◽  
Filter Frequency

scholarly journals Tectono-Stratigraphic Note: Time calibration of late Carboniferous, Permian and Early Triassic Arabian stratigraphy to orbital-forcing predictions

GeoArabia ◽  
2005 ◽  
Vol 10 (2) ◽  
pp. 189-192 ◽  
Author(s):  
Moujahed Al-Husseini ◽  
Robley K. Matthews
Keyword(s):  
Second Order ◽  
Late Carboniferous ◽  
Orbital Forcing ◽  
Third Order ◽  
Depositional Sequence ◽  
Sequence Stratigraphic ◽  
Rosetta Stone ◽  
Time Calibration ◽  
Sequence Boundaries ◽  
Order Sequence

The recent publication of GTS 2004 (Gradstein et al., 2004) provides an opportunity to recalibrate in time the late Carboniferous, Permian and Early Traissic Arabian Stratigraphy (GeoArabia Special Publication 3, Edited by Al-Husseini, 2004) as represented by the rock units in subsurface Interior Oman (Osterloff et al., 2004a, b) and the Haushi-Huqf Uplift region (Angiolini et al., 2004) (Figure). Additionally, sequence stratigraphic models of orbital forcing (Matthews and Frohlich, 2002; Immenhauser and Matthews, 2004) provide new insights in regards to the time calibration of depositional sequences: the “Rosetta Stone” approach. The Rosetta Stone approach predicts that the period of a third-order depositional sequence is 2.430 ± 0.405 my (denoted DS3 and here adjusted to increase the fourth-order ‘geological tuning fork’ from 0.404 to 0.405 my based on Laskar et al., 2004). The present calibration is also tied to the orbital-forcing model developed by R.K. Matthews (in Al-Husseini and Matthews, 2005; this issue of GeoArabia) that predicts that a second-order depositional sequence (denoted DS2) consists of six DS3s that were deposited in a period of about 14.58 my (6 x 2.430 my); the DS2 being bounded by two regional second-order sequence boundaries (SB2) corresponding to sea-level maximum regression surfaces.

Second-Order Sequence Stratigraphic Controls on the Quality of the Fossil Record at an Active Margin: New Zealand Eocene to Recent Shelf Molluscs

Palaios ◽  
2006 ◽  
Vol 21 (1) ◽  
pp. 86-105 ◽  
Author(s):  
J. S. CRAMPTON ◽  
M. FOOTE ◽  
A. G. BEU ◽  
R. A. COOPER ◽  
I. MATCHAM ◽  
...  
Keyword(s):  
New Zealand ◽  
Fossil Record ◽  
Second Order ◽  
Active Margin ◽  
Sequence Stratigraphic ◽  
Order Sequence

Sedimentary Facies of the First Member of Qingshankou-Formation in Late Cretaceous Songliao Basin of Daqing Oilfield China

2014 ◽  
Vol 898 ◽  
pp. 428-431
Author(s):  
Qian Zhang
Keyword(s):  
Sedimentary Facies ◽  
Second Order ◽  
Songliao Basin ◽  
Third Order ◽  
Sequence Stratigraphic ◽  
Core Logging ◽  
The One ◽  
Continental Basin ◽  
Order Sequence ◽  
Sequence Unit

According to core, logging and seismic data, using tectonic-stratigraphic and sequence stratigraphic analysise theories in Qingshankou Formation of division and comparison, and the sequence boundary and sequence unit to be optimized, in order to carry out seismic deposition. By determining the levels of sequence interface on seismic, logging and faces reflecting characteristics of the study area to build sequence interface identifier. In the course of practical work, identified the continental basin of the more common of the one to three levels of sequence interface, system interface and the parasequence set interface. In Songliao Basin, second-order sequences often corresponding to the tectonic evolution of the basin episodic stage, and in each period of prototype basin internal episodic tectonic extension or episodic of tectonic inversion is consistent, in Qingshankou Formation in the development of one second-order sequence boundary SB11 (T11), three third-order sequence boundary, there are SB12 (T12), SB13 (T13) and SB2 (T2), seven forth-order sequence boundary. In the plane, using the data of 256 wells, analysis of the distribution characteristics of the sedimentary facies of the first member of Qingshankou-Formation.

Transgressive–regressive (T–R) sequence analysis of the Jurassic succession of the Sverdrup Basin, Canadian Arctic Archipelago

1993 ◽  
Vol 30 (2) ◽  
pp. 301-320 ◽  
Author(s):  
A. F. Embry
Keyword(s):  
Sequence Analysis ◽  
Sea Level ◽  
Second Order ◽  
Sea Level Changes ◽  
Third Order ◽  
Sverdrup Basin ◽  
Sequence Boundaries ◽  
Boundary Characteristics ◽  
Fifth Order ◽  
Order Sequence

Transgressive–regressive (T–R) sequence analysis has been applied to the Jurassic succession of the Sverdrup Basin with sequence boundaries drawn at subaerial unconformities or the correlative transgressive surfaces. A hierarchal system of sequence order that reflects the different nature of the boundaries has been formulated on the basis of boundary characteristics. Second- through fifth-order sequences have been recognized in the Jurassic succession, which itself is part of a first-order sequence of mid-Permian – Early Cretaceous age.The Jurassic strata occur within four second-order sequences. The boundaries of these sequences are characterized by widespread subaerial unconformities across which major changes in depositional and subsidence regimes occur. These boundaries are earliest Rhaetian, earliest Pliensbachian, earliest Bajocian, earliest Oxfordian, and Hauterivian in age.Each second-order sequence is divisible into a number of third-order sequences bounded mainly by basin-wide transgressive surfaces with subaerial unconformities present on the basin margins. The ages of the 10 Jurassic third-order sequences are Rhaetian – Hettangian, Sinemurian, Pliensbachian – Toarcian, late Toarcian – Aalenian, Bajocian, Bathonian, Callovian, Oxfordian – early Kimmeridgian, late Kimmeridgian – early Tithonian, and late Tithonian. The third-order sequences commonly contain three to six fourth-order sequences. These sequences are bound entirely by transgressive surfaces that can be correlated only over a portion of the basin.A good correlation between the second- and third-order transgressive events of the Sverdrup Basin and proposed global events is observed. This worldwide occurrence suggests that the events in part reflect eustatic sea-level changes. The characteristics of the second- and third-order boundaries also indicate that each had a tectonic influence that resulted in a rapid relative sea-level fall (uplift) followed by a rapid rise (subsidence). Given the apparent combination of tectonic and eustatic influence on the generation of the second- and third-order sequence boundaries, they are interpreted to reflect significant plate-tectonic reorganizations that affected the intraplate stress regimes of the oceanic (eustatic) and continental (tectonic) portions of each lithospheric plate.

scholarly journals Stratigraphic Note: Orbital calibration of the Arabian Jurassic second-order sequence stratigraphy

GeoArabia ◽  
2006 ◽  
Vol 11 (3) ◽  
pp. 161-170 ◽  
Author(s):  
Moujahed Al-Husseini ◽  
Robley K. Matthews
Keyword(s):  
Sequence Stratigraphy ◽  
Second Order ◽  
Order Sequence

scholarly journals Devonian Jauf Formation, Saudi Arabia: Orbital Second-order Depositional Sequence 28

GeoArabia ◽  
2006 ◽  
Vol 11 (2) ◽  
pp. 53-70 ◽  
Author(s):  
Moujahed Al-Husseini ◽  
Robley K. Matthews
Keyword(s):  
Saudi Arabia ◽  
Second Order ◽  
Third Order ◽  
Depositional Sequence ◽  
Early Devonian ◽  
Orbital Cycles ◽  
Flooding Event ◽  
Sequence Boundaries ◽  
Order Sequence ◽  
Reference Section

ABSTRACT The Devonian Jauf Formation (Huj Group) froms part of a regional transgressive-regressive depositional sequence that extends more than 1,500 km across the Arabian Platform from the Al Jawf outcrops in northwest Saudi Arabia, to the subsurface of eastern Saudi Arabia and Oman (Misfar Group). The formation ranges in thickness from 200–335 m in eastern Saudi Arabia to about 300–330 m in northwest Saudi Arabia. It disconformably (?unconformably) overlies the continental to shallow-marine Tawil Formation, and is unconformably overlain by the continental Jubah Formation. The Jauf Formation consists of five members that are apparently conformable; from base-up: Sha’iba Shale, Qasr Limestone, Subbat Shale, Hammamiyat Limestone and Murayr. In the Al-Qalibah reference section, it is divided into 21 informal units. The Early Devonian Emsian Hammamiyat Member represents the main marine flooding event; it consists of Hammamiyat units 1–6 each characterized by a clastic section that is capped by limestone. The Jauf Formation is interpreted as an orbital second-order depositional sequence (denoted DS2 28), which is bounded by two second-order sequence boundaries: SB2 28 = Jauf/Tawil (c. 407.6 Ma) and SB2 27 = Jubah/Jauf (c. 393.0 Ma). The Jauf Formation appears to consist of six third-order depositional sequences (DS3 28.1 to 28.6) that were deposited in the Early Devonian, ?Pragian and Emsian stages The Hammamiyat Member (DS3 28.4) is interpreted to consist of six fourth-order orbital cycles (DS4 28.4.1 to 28.4.6) each deposited in 0.405 million years.

SEQUENCE STRATIGRAPHY AND HYDROCARBON PROSPECTIVITY OF THE CAMPANIAN TO EOCENE SUCCESSION, NORTHERN BONAPARTE BASIN, AUSTRALIA

1998 ◽  
Vol 38 (1) ◽  
pp. 313 ◽  
Author(s):  
C.L. Mclntyre ◽  
P.J. Stickland
Keyword(s):  
Second Order ◽  
Carbonate Ramp ◽  
Sediment Supply ◽  
Passive Margin ◽  
Third Order ◽  
Carbonate System ◽  
Valley Fill ◽  
Early Paleocene ◽  
Order Sequence ◽  
Migration Pathways

The Campanian to Eocene succession of the Northern Bonaparte Basin contains a number of siliciclastic reservoirs which provide alternative targets to the Callovian structural plays that have dominated exploration to date. The succession is part of the Passive Margin Megasequence which extends from the Aptian to the Pliocene, and is traditionally subdivided into the Turnstone, Johnson and Grebe Formations.Prograding deltaics of the Turnstone Formation swamped an incipient Early-Campanian carbonate ramp following a second-order sequence-boundary. Five third-order sequences are recognised within the Turnstone Formation, each dominated by Lowstand (shelf-margin wedge) and Highstand Systems Tract components. A coeval basinal carbonate system resulted in the deposition of marls and lutites distal of the clastic deltaics. In the Early Paleocene, drowning of the clastic system led to the establishment of a productive carbonate ramp. Rare lowstand siliciclastic reservoirs are developed within carbonate-dominated prograding complexes, as incised valley-fill, and possibly within prominent slope canyons. In the Late Paleocene, a third-order transgression drowned the carbonate system. The Early Eocene Grebe sandstones were then deposited as a second-order lowstand package upon a prominent sequence-boundary. Subsequent flooding of the siliciclastic system resulted in the re-establishment of the prograding carbonate ramp system.The morphology of the passive-margin was strongly influenced by the interplay between sediment-supply and subsidence. The predominantly ramp-like geometry of the margin promoted the development of numerous shallow-marine lowstand reservoirs. The hydrocarbon prospectivity of each of these reservoirs is primarily controlled by the magnitude of the subsequent flooding events: Only the largest transgressions resulted in sufficient reduction of depositional energy to isolate the lowstand siliciclastics.Vertical migration remains the critical risk for all passive margin plays, as the reservoirs are separated from the Late Jurassic and Early Cretaceous source kitchens by up to one kilometre of claystone dominated sequences. None-the-less, the widespread occurrence of shallow hydrocarbon shows in the greater Bonaparte Basin indicates that Neogene faulting does provide locally valid migration pathways into post-rift reservoirs.

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