The aim of this paper is to investigate the control of chaotic Burke-Shaw system using Pyragas method. This system is derived from Lorenz system which has several applications in physics and engineering (e.g. secure communications). The linear stability and the existence of Hopf bifurcation of this system are investigated. Based on the characteristic equation, a theorem is stated and proved. This theorem is used to calculate the interval values of the time delay $ au $ at which this system is stable (unstable). By establishing appropriate time delay $ au $ and feedback strength $K$ ranges, one of the unstable equilibria of this system can be controlled to be stable. We, also, introduced the fractional version of this system which is not studied in the literature as far as we know. The advantage of the fractional order system is that, the system has extra parameter which enriches its dynamics. Increasing the number of parameters may be used to increase the security of the transmitted information. We apply the Pyragas method to control the chaotic behavior of fractional Burke-Shaw system. As we did for the integer order, we determine the values of $ au $ and $K$ which guarantee that the fractional version is stable. Finally, to support the analytical results, some numerical simulations are carried out which indicate that chaotic solution is turned to be stable if $ au $ passes through certain intervals. The bifurcation diagrams are calculated.

In this paper we introduce the concept of generalized fuzzy soft mappings on families of generalized fuzzy soft sets and study the properties of generalized fuzzy soft images ( inverse images) of generalized fuzzy soft sets. Furthermore, generalized fuzzy soft continuous mappings, generalized fuzzy soft open (closed) mappings and generalized fuzzy soft homeomorphisms are introduced.

In this paper we introduce the concept of generalized fuzzy soft mappings on families of generalized fuzzy soft sets and study the properties of generalized fuzzy soft images ( inverse images) of generalized fuzzy soft sets. Furthermore, generalized fuzzy soft continuous mappings, generalized fuzzy soft open (closed) mappings and generalized fuzzy soft homeomorphisms are introduced.

The Campanian-Eocene succession exposed at Wadi Tarfa and north Wadi Qena area, north Eastern Desert, Egypt is differentiated from base to top into: the pre-Middle Campanian (Santonian?) Rakhiyat Formation (R), the Middle Campanian-Late Maastrichtian Sudr Formation (S), the redefined Late Danian-Early Thanetian Beida Formation (B), the Early Late Thanetian Tarawan Formation (T), the Latest Late Thanetian-Lower Ypresian Esna Formation (Es), the Late Lower Ypresian-Late Upper Ypresian Thebes Formation (Th) and the newly recorded Middle Lutetian El Mereir Formation (M). The ages given here for the rock units depend on a high resolution planktonic foraminiferal zonation. Field observations, beside the microfacies and benthonic paleobathymetric investigations, helped also in reaching a third order resolution of these sequences into their lowstand, transgressive, regressive and highstand systems tracts.

The Campanian-Eocene succession exposed at Wadi Tarfa and north Wadi Qena area, north Eastern Desert, Egypt is differentiated from base to top into: the pre-Middle Campanian (Santonian?) Rakhiyat Formation (R), the Middle Campanian-Late Maastrichtian Sudr Formation (S), the redefined Late Danian-Early Thanetian Beida Formation (B), the Early Late Thanetian Tarawan Formation (T), the Latest Late Thanetian-Lower Ypresian Esna Formation (Es), the Late Lower Ypresian-Late Upper Ypresian Thebes Formation (Th) and the newly recorded Middle Lutetian El Mereir Formation (M). The ages given here for the rock units depend on a high resolution planktonic foraminiferal zonation. Field observations, beside the microfacies and benthonic paleobathymetric investigations, helped also in reaching a third order resolution of these sequences into their lowstand, transgressive, regressive and highstand systems tracts.

The Campanian-Eocene succession exposed at Wadi Tarfa and north Wadi Qena area, north Eastern Desert, Egypt is differentiated from base to top into: the pre-Middle Campanian (Santonian?) Rakhiyat Formation (R), the Middle Campanian-Late Maastrichtian Sudr Formation (S), the redefined Late Danian-Early Thanetian Beida Formation (B), the Early Late Thanetian Tarawan Formation (T), the Latest Late Thanetian-Lower Ypresian Esna Formation (Es), the Late Lower Ypresian-Late Upper Ypresian Thebes Formation (Th) and the newly recorded Middle Lutetian El Mereir Formation (M). The ages given here for the rock units depend on a high resolution planktonic foraminiferal zonation. Field observations, beside the microfacies and benthonic paleobathymetric investigations, helped also in reaching a third order resolution of these sequences into their lowstand, transgressive, regressive and highstand systems tracts.

The Campanian-Eocene succession exposed at Wadi Tarfa and north Wadi Qena area, north Eastern Desert, Egypt is differentiated from base to top into: the pre-Middle Campanian (Santonian?) Rakhiyat Formation (R), the Middle Campanian-Late Maastrichtian Sudr Formation (S), the redefined Late Danian-Early Thanetian Beida Formation (B), the Early Late Thanetian Tarawan Formation (T), the Latest Late Thanetian-Lower Ypresian Esna Formation (Es), the Late Lower Ypresian-Late Upper Ypresian Thebes Formation (Th) and the newly recorded Middle Lutetian El Mereir Formation (M). The ages given here for the rock units depend on a high resolution planktonic foraminiferal zonation. Field observations, beside the microfacies and benthonic paleobathymetric investigations, helped also in reaching a third order resolution of these sequences into their lowstand, transgressive, regressive and highstand systems tracts.

The Campanian-Eocene succession in Gabal Oweina area, Upper Egypt, covering six rock units (Quseir, Duwi, Dakhla, Tarawan, Esna and Thebes formations) was revised. The sedimentological and biostratigraphical detailed studies of the succession helped in reaching a high-resolution sequence stratigraphic classification that led to the recognition of five third-order depositional sequences and their associated surfaces and systems tracts. Also, the paleobathymetry deduced from the identified benthonic faunal assemblages, helped in giving some details about the characteristics and paleoenvironments of the identified sequences. The Campanian depositional sequence Dw/DkSQ1, includes both the Duwi and the lower part of the Dakhla formations, was laid down in a sea oscillating between inner to middle neritic depths, on shallow subtidal shelf, followed by a shallow inner neritic depths, on lagoonal environment. The Maastrichtian depositional sequence DkSQ2 encompass the middle part of the Dakhla Formation and was laid down in a relatively outer neritic to upper bathyal depths, on deep subtidal shelf, followed by inner neritic depths, on a shallow subtidal shelf at the end of the sequence marked by an intraformational conglomerate bed. The Danian depositional sequence DkSQ3 covers the upper part of the Dakhla Formation and started by a latest Maastrichtian- earliest Danian hiatus. It accumulated in gradually deepening waters reaching upper bathyal depths, on deep subtidal shelf, followed by middle neritic depths, on a shallow subtidal shelf. The Selandian-Thanetian depositional sequence Dk/T/EsSQ4 comprises the uppermost part of the Dakhla, Tarawan and the lower part of the Esna formations and began by Danian-Selandian hiatus. It accumulated in oscillating conditions between upper bathyal depths, on a deep subtidal shelf to middle neritic depths, on a shallow subtidal shelf. The Ypresian depositional sequence EsSQ5 consists of the main parts of the Esna Formation and initiated by Paleocene/Eocene hiatus. It was laid down in a gradually deepening sea reaching the deep upper bathyal depths on a deep subtidal shelf, before reaching shallow middle neritic depths on a shallow subtidal shelf. Four of the recognized five sequence boundaries (SB1, SB3, SB4 and SB5) coincide with global sea-level falls, while the other one (SB2) is related to a local tectonic in the studied area.

The Campanian-Eocene succession in Gabal Oweina area, Upper Egypt, covering six rock units (Quseir, Duwi, Dakhla, Tarawan, Esna and Thebes formations) was revised. The sedimentological and biostratigraphical detailed studies of the succession helped in reaching a high-resolution sequence stratigraphic classification that led to the recognition of five third-order depositional sequences and their associated surfaces and systems tracts. Also, the paleobathymetry deduced from the identified benthonic faunal assemblages, helped in giving some details about the characteristics and paleoenvironments of the identified sequences. The Campanian depositional sequence Dw/DkSQ1, includes both the Duwi and the lower part of the Dakhla formations, was laid down in a sea oscillating between inner to middle neritic depths, on shallow subtidal shelf, followed by a shallow inner neritic depths, on lagoonal environment. The Maastrichtian depositional sequence DkSQ2 encompass the middle part of the Dakhla Formation and was laid down in a relatively outer neritic to upper bathyal depths, on deep subtidal shelf, followed by inner neritic depths, on a shallow subtidal shelf at the end of the sequence marked by an intraformational conglomerate bed. The Danian depositional sequence DkSQ3 covers the upper part of the Dakhla Formation and started by a latest Maastrichtian- earliest Danian hiatus. It accumulated in gradually deepening waters reaching upper bathyal depths, on deep subtidal shelf, followed by middle neritic depths, on a shallow subtidal shelf. The Selandian-Thanetian depositional sequence Dk/T/EsSQ4 comprises the uppermost part of the Dakhla, Tarawan and the lower part of the Esna formations and began by Danian-Selandian hiatus. It accumulated in oscillating conditions between upper bathyal depths, on a deep subtidal shelf to middle neritic depths, on a shallow subtidal shelf. The Ypresian depositional sequence EsSQ5 consists of the main parts of the Esna Formation and initiated by Paleocene/Eocene hiatus. It was laid down in a gradually deepening sea reaching the deep upper bathyal depths on a deep subtidal shelf, before reaching shallow middle neritic depths on a shallow subtidal shelf. Four of the recognized five sequence boundaries (SB1, SB3, SB4 and SB5) coincide with global sea-level falls, while the other one (SB2) is related to a local tectonic in the studied area.

The Campanian-Eocene succession in Gabal Oweina area, Upper Egypt, covering six rock units (Quseir, Duwi, Dakhla, Tarawan, Esna and Thebes formations) was revised. The sedimentological and biostratigraphical detailed studies of the succession helped in reaching a high-resolution sequence stratigraphic classification that led to the recognition of five third-order depositional sequences and their associated surfaces and systems tracts. Also, the paleobathymetry deduced from the identified benthonic faunal assemblages, helped in giving some details about the characteristics and paleoenvironments of the identified sequences. The Campanian depositional sequence Dw/DkSQ1, includes both the Duwi and the lower part of the Dakhla formations, was laid down in a sea oscillating between inner to middle neritic depths, on shallow subtidal shelf, followed by a shallow inner neritic depths, on lagoonal environment. The Maastrichtian depositional sequence DkSQ2 encompass the middle part of the Dakhla Formation and was laid down in a relatively outer neritic to upper bathyal depths, on deep subtidal shelf, followed by inner neritic depths, on a shallow subtidal shelf at the end of the sequence marked by an intraformational conglomerate bed. The Danian depositional sequence DkSQ3 covers the upper part of the Dakhla Formation and started by a latest Maastrichtian- earliest Danian hiatus. It accumulated in gradually deepening waters reaching upper bathyal depths, on deep subtidal shelf, followed by middle neritic depths, on a shallow subtidal shelf. The Selandian-Thanetian depositional sequence Dk/T/EsSQ4 comprises the uppermost part of the Dakhla, Tarawan and the lower part of the Esna formations and began by Danian-Selandian hiatus. It accumulated in oscillating conditions between upper bathyal depths, on a deep subtidal shelf to middle neritic depths, on a shallow subtidal shelf. The Ypresian depositional sequence EsSQ5 consists of the main parts of the Esna Formation and initiated by Paleocene/Eocene hiatus. It was laid down in a gradually deepening sea reaching the deep upper bathyal depths on a deep subtidal shelf, before reaching shallow middle neritic depths on a shallow subtidal shelf. Four of the recognized five sequence boundaries (SB1, SB3, SB4 and SB5) coincide with global sea-level falls, while the other one (SB2) is related to a local tectonic in the studied area.