Tarek Askri

Zied Hajej

Nidhal Rezg

An Optimal Integrated Maintenance for Multi Parallel Workstations Under Returned Products

Keywords: Production and maintenance planning, preventive maintenance, minimal repair, Service level, Multi parallel leased machines, returned products Asymmetry Coefficient. c o : Overtime cost c n : Cost of unused normal time c h : Inventory cost. M p : unit preventive maintenance cost M c : unit corrective maintenance cost 2) Problem description

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I. INTRODUCTION

Random Failure, random demand, availability and reliability of equipment's are considered among the uncertainties that influenced on the production and maintenance policies of manufacturing systems. Facing these uncertainties, the companies choose a policy of collaboration and cooperation with other enterprises. In this context, the leasing is considered as a best solution in term of cost since more industries have preferred leasing rather than owning it. [START_REF] Pongpech | Optimal periodic preventive maintenance policy for leased equipment[END_REF] shows the importance of the leasing and presented the causes of equipment leasing that the cost of purchase of new equipment is increasing.

Concerning maintenance while leasing equipment, [START_REF] Yeh | Optimal number of leased periods and maintenance policy with threshold value on age for leased equipment[END_REF] considered a mathematical formulation for a maintenance policy characterized by a minimal repair in the case fails of equipment. When the equipment age spreads a certain threshold value, an imperfect preventive maintenance is approved. Finally, they illustrated the effects of the number of lease periods and the maintenance strategy on the total cost by a numerical example. Recently, [START_REF] Chang | Joint determination of lease period and preventive maintenance policy for leased equipment with residual value[END_REF] proposed an analytical study and a numerical example in order to obtain the optimal maintenance policy and the length of the lease period by showing the impact of the optimal lease period and the maintenance strategy for profit model. Concerning production and maintenance optimization of single or multiple manufacturing machines, [START_REF] Kenne | Simultaneous control of production, preventive and corrective maintenance rates of failure prone manufacturing system[END_REF] proposed and minimized a mathematical model of manufacturing system of numerous identical workstations and subjected to reparation periods, in order to control the production level and the reparation date. [START_REF] Nkeungoue | Simultaneous control of production, preventive and corrective maintenance rates of failure prone manufacturing system[END_REF] minimized a total production and maintenance cost for production system of various workstations considering the failure prone manufacturing system. [START_REF] Hu | Optimality of hedging point policies in the production control of failure prone manufacturing systems[END_REF] treated the optimality of a production system using the hedging point policy which the machine failure rate be determined by the production level. [START_REF] Rezg | Joint optimization of pre ventive maintenance and inventory control in a production line using simulation[END_REF] proposed a jointly stock and maintenance optimization in a production system of numerous machines.

This work is the continuation of [START_REF] Medhioub | A stochastic production planning optimization for multi parallel machine under leasing Contract[END_REF] and [START_REF] Zied | A production planning optimization for multi parallel machine under withdrawal right[END_REF] works. [START_REF] Medhioub | A stochastic production planning optimization for multi parallel machine under leasing Contract[END_REF] dealt with a production scheme contains numerous similar workstations which has to meet a random demand respecting a certain service level. The objective is to determine the optimal production plan characterized by the optimal number of machine, facility time and inventory levels. [START_REF] Zied | A production planning optimization for multi parallel machine under withdrawal right[END_REF] deals the same problem of [START_REF] Medhioub | A stochastic production planning optimization for multi parallel machine under leasing Contract[END_REF] considering the influence of the returned product by the market on the optimization problem. In our work, we propose a production and maintenance strategies where the production rate depend to the returned products and the maintenance strategy be determined according to the economical production plan where the degradation of equipment is influenced by the variation of production rates. Consequently, an optimal combination of workstations amount, manufacture level, and inventory levels is proposed to meet the random demand under facility level. A maintenance strategy is developed to establish the optimum number of preventive maintenance actions for all leased machines by minimizing the total maintenance cost.

This paper is planned as follow: Section II proposes the methodology followed and discusses the mathematical model of production system by presenting the different costs. Section III presents a simple numerical example and gives the results. Discussions are proposed in section IV.

II. PRODUCTION AND MAINTENANCE FORMULATION

A. Production Planning 1) Notations H. ∆t : finite production time horizon. ∆t: production period δ : rate of returned product .

An Optimal Integrated Maintenance for Multi Parallel Workstations Under Returned Products

T. Askri, Z. Hajej, N. Rezg Université de Lorraine, Metz, France tarek.askri@univ-looraine.fr, zied.hajej@univ-lorraine.fr, nidhal.rezg@univ-lorraine.fr This study consists with production system a several parallel leased machines that produces periodically one type of product. The random demands are satisfied from the store S during a finite production horizon. The customer demands are random and characterized by a Gaussian distribution with first and second statistical moments given respectively, by d and σ d 2 . The satisfaction of the request is made at the end of each period under a given service level θ. The production system takes into account the withdrawal right where the customers have the right to return a quantity of products to stock S provided that it still in new and saleable conditions, before a fixed deadline τ r . The normal work hours of each machine is characterize by a upper bound time units max N X for each production period and the overtime of each machine, when the amount of demand is greater to production quantity, not exceeds the upper bound of time units ax S m X . The production system is characterize by the variation of leasing workstations number between the different productions periods according to the amount of returned product from market and production rates. The goal is to determine an optimal production plan and an optimal maintenance strategy. The production policy characterized by the variation of leased machines number and the returned products constraint. The impact of withdrawal right is justified by the impact returned production on the production system and consequently on the maintenance plan whose the degradation degree of machines influenced by the production rates.

3) Problem formulation

The decision variables of the stochastic model are the number of leased machines and the production rate

Δ N S k i k i k M X X k k k h k k M S k i k i CT c M c c M M c c S a a d c θ t X - = ⋅ + ⎡ ⎤ ⎣ ⎦ ⎡ ⎤ + - - ⎢ ⎥ ⎣ ⎦ ⎡ ⎤ + × -+ × ⎢ ⎥ ⎣ ⎦ = + × × × ( ) ( ) 1 • Cost of overtime work max 1 Cost of unexploited capacities 1 Δ max 0, k k H k M N N k n i k i θ c t X X = = ⎧ ⎫ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎨ ⎬ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎡ ⎤ + -× × × - ⎪ ⎪ ⎣ ⎦ ⎪ ⎪ ⎪ ⎪ ⎪ ⎪ ⎩ ⎭ ∑ ∑ ∑ Subject to 1 k k k k k S S U d r - = + - + (1) with
,....., k H = - 1 1
( ) 0 r r k t d i f k r k o t h e r w i s e τ δ τ ⎛ ⎞ - ⎜ ⎟ Δ ⎝ ⎠ ⋅ ≥ ⎧ ⎪ = ⎨ ⎪ ⎩ (2)
,.....,

k H = - 1 1 , Δ r τ h t = ⋅ and 1 h ≥ ( ) 1 Δ K W N S k i k i k i U u t X X = = × × + ∑ (3)
( )

P r o b 0 k S ≥ ≥ α (4) k m M M ≤ ≤ (5) m a x 0 N N i k X X ≤ ≤ (6) m a x 0 S S i k X X ≤ ≤ (7)
Where the relation (1) describes the cumulative equation of inventory for each period k take into account the quantity of returned product. The constraint (2) represents the product amount returned from the market after a specific deadline. The equation (3) computes the production rate at each production period depending to the work times of each workstations and the production quantity of each machine. The service level for each period is given by the constraint (4). The constraint [START_REF] Kenne | Simultaneous control of production, preventive and corrective maintenance rates of failure prone manufacturing system[END_REF] defines the upper and lower number of leased machines at each production period. Finally, the last constraints ( 6) and ( 7) define the upper and lower bound of normal and over time work variables.

B. Analytical Study

In this section, we proposed an analytical study in order to simplify the expected total cost by transforming our stochastic problem to a deterministic corresponding problem. The mean variables are following:

{ } , , î k i k E S S = ; { } k k E U U = ; { } k k E M M = ; { } N N ik ik E X X = ; { } S S ik ik E X X =
And the variances:

0 U k V = , 0 W k V = , 0 N X ik V = , 0 S X ik V = .
We can obtain the simplified cost:

( ) ( ) ( ) ( ) ( ) ( ) ( ) ( ) ( ) ( ) ( )
2 1 2 3 1 4 1 max , 1 1 2 1 2 2 2 2 2 Δ 1 Δ max 0, 1 1 1 2 2 k k k k k k M S o k ik i H M N N k n ik M U k i h k k d d c M c c M M c c θ t X Min θ c t X X c S a a d H H a V H a V H - = = = ⎛ ⎞ ⎧ ⎫ ⋅ + + ⋅ - - ⎜ ⎟ ⎪ ⎪ ⎜ ⎟ ⎪ ⎪ ⎜ ⎟ ⎪ ⎪ + ⋅ ⋅ ⋅ ⎜ ⎟ ⎪ ⎪ ⎜ ⎟ ⎪ ⎪ ⎨ ⎬ ⎜ ⎟ ⎪ ⎪ ⎜ ⎟ ⎡ ⎤ + -⋅ ⋅ ⋅ - ⎪ ⎪ ⎜ ⎟ ⎣ ⎦ ⎪ ⎪ ⎜ ⎟ ⎪ ⎪ ⎜ ⎟ + ⋅ -+ ⋅ ⎪ ⎪ ⎜ ⎟ ⎩ ⎭ ⎜ ⎟ ⎜ ⎟ + + ⋅ ⋅ ⋅ + + ⋅ ⋅ ⋅ - ⎜ ⎟ ⎝ ⎠ ∑ ∑ ∑ (8)
With as:

1 Δ 1 r k k k r k t k k k k r S U d If k S S U d If k d - ⎛ ⎞ - ⎜ ⎟ ⎝ ⎠ - ⎧ + + - ≥ ⎪ ⎪ = ⎨ ⎪ + - < ⎪ ⎩ ⋅ τ τ τ δ (9) • Chance-constraint
The difficulty of solving this stochastic problem optimization requires us to converted the chanceconstraint characterized the service level to equivalent deterministic problem that preservers original properties.

( )

1 ( 1 ) Pr 0 0,1,...., 1 ˆˆr k k k k k k U V V d d ob S k H k r S d d τ α ϕ α τ δ - - ⎛ ⎞ ⎛ ⎞ ⎜ ⎟ ⎜ ⎟ ⎜ ⎟ ⎜ ⎟ ⎜ ⎟ ⎜ ⎟ ⎝ ⎠ ⎜ ⎟ ⎜ ⎟ ⎝ ⎠ - ≥ × × ≥ ≥ ⇒ = - - -+ -⋅ (10) ϕ is a Gaussian cumulative distribution function with mean , 1 . ˆr k d k d V V d d k r τ δ τ - - ⋅ - and finite variance 2 2 , , , 1 . 0 r r d k d k d k d V V V V τ τ δ - - ⎛ ⎞ ⎛ ⎞ ⎛ ⎞ ⎜ ⎟ + ≥ ⎜ ⎟ ⎜ ⎟ ⎜ ⎟ ⎜ ⎟ ⎝ ⎠ ⎝ ⎠ ⎝ ⎠ - ⋅ .

C. Maintenance Planning Problem

Considering the developed production planning, we are able to determine the maintenance strategy which allows minimizing its total cost. We assumed in the maintenance strategy a preventive maintenance action with minimal overhaul practiced in periods (h×T) (h= 1, 2 ...).

Assuming that the times of repair and replacements are negligible, the aim of the maintenance strategy is to determine the optimal number of preventive maintenances N * that minimize the total cost as well as the minimal preventive maintenance interval. The relationship between N * and T * is given by: ( )

* * 1 H N T ⎢ ⎥ - = ⎢ ⎥ ⎣ ⎦ ( 11
)
Assuming that the machines degradation is linear and the failure rate is increased according to time and production level.

Dealing with multiple leased machines, the evolution of the equipment failure rate is presented as follows:

[ ]

( 1) max ( ) . ( ) . ( ) 0, ik ik ik i k n p k t C k t t t u λ λ λ - Δ = Δ + ∀∈ Δ ( 12
)
Where:

( ) n t λ represents the nominal workstation failure rate ik p represents the quantity of product for workstation i at period k ( )

Δ N S ik ik ik p k u X X = × × + ( 13
)
max u is the maximum production rate of a workstation ( )

m a x m a x m a x Δ N S u X X u t × + = ik
C is a binary variable presented as follows:

1 if workstation i has been used during period k-1

0 if no ik C = ⎧ ⎨ ⎩
The total maintenance cost is formed by two cost functions related to preventive and corrective maintenance actions and is expressed as follows:

1 .

1 1 . 1 ( ) ( ) jT H M j T T p i p c j i p j T q T M C M An T ϕ - ⎢ ⎥ ⎢ ⎥ ⎣ ⎦ = = = -+ ⎛ ⎞ = × + × ⎜ ⎟ ⎝ ⎠ ∑ ∑ ∏ ( 14
)
For the preventive maintenance cost is given by the unit maintenance cost multiply by the number of machine on which the maintenance will be applied.

We assume that preventive actions should not be performed on all machines used in period j.T * but only in machines used at last in q periods with 1 2

2 i f T q i f n o ≤ ⎧ = ⎨ ⎩
The second part of total maintenance cost is the corrective maintenance cost where ( ) An T represents the average number of failures until the last preventive action and considering the periods j∈ {1, 2, .., N T } and during the last periods ∈ {N T+ 1 , N T+ 2 , .., H }.

( )

An T is formulated as follows:

(

. 1 1 1 0 0 . 1 ( ) ( ) ( ) k k H t t M M j T T H ik ik H j k jT i i k T T An T t dt t dt λ λ - ⎢ ⎥ - ⎢ ⎥ Δ Δ + ⎣ ⎦ - = = + = = ⎢ ⎥ = + ⎢ ⎥ ⎣ ⎦ = + ∑ ∑ ∑ ∑ ∑ ∫ ∫ (15) Where: ( ) ( ) ( ) ( ) ( ) [ ] 1 1 Δ 1 ' ' 1 max max 1 Δ Δ ; 0,Δ k i k ip k k ik p p n n i p p j T P P k λ t C λ t λ t t t u u - - = ⋅ + = ⋅ + ⎡ ⎤ ⎢ ⎥ = ∏ × + × ∈ ⎢ ⎥ ⎢ ⎥ ⎣ ⎦ ∑ And ( ) 1 1 2 1 ( ' 1 ) ' 1 max max . 1 ( ) ( ) ( ) ip ik k k ik p n n p p H p p p k k t C t t u u α α λ λ λ = = + = - ⎢ ⎥ = + ⎢ ⎥ ⎢ ⎥ ⎣ ⎦ ⎡ ⎤ ⎢ ⎥ ⎛ ⎞ Δ Δ = × × Δ+ × ⎢ ⎥ ⎜ ⎟ ⎝ ⎠ ⎢ ⎥ ⎢ ⎥ ⎣ ⎦ ∑ ∏ III. RESULTS 1 ) 1 ( 1). 1 2 ( 1) 0
Using the models described in previous section, a numerical example is presented to determine the economical production plan and the optimal maintenance strategy. The production horizon H is equal to 5 periods and the length of each period ∆t is equal to 25 days duration. with σ d =1. For the maintenance strategy, using the results of the production planning, the maintenance scheduling can now be improved with M p = 500 mu and M c = 2000 mu The machine number vector with these production inputs and considering δ=0.1 (optimal value of returned products) is illustrated as follows: M k =(7,8,7,7,8)

We assume that the nominal failure rate function follows a Weibull distribution given by: 1 ( )

γ n γ t λ t β β - ⎛ ⎞ = ⋅ ⎜ ⎟ ⎝ ⎠
With these parameters α=2 and β=100.

According to the units costs of preventive and maintenance actions, we obtained the optimal preventive maintenance interval T * as well as the optimal number of preventive maintenance actions N*. From figure 2, we can conclude that the optimal preventive maintenance interval is equal to T*=2 where we obtain the lowest maintenance cost that equal to ϕ(T*)=28000 um. And in this case, we can apply two preventive maintenance actions (N*=2);

IV. DISCUSSION

According to the results given in the previous section, we can note that more the interval between preventive maintenance actions is high more the maintenance total cost is increasing. In fact, the machines to which preventive actions are not applied are more subjects to breakdowns. Then, expensive corrective actions are applied. Otherwise, in the case of applying preventive actions more frequently, it also leads to increase the total maintenance cost.

V. CONCLUSION

This study presented a stochastic production and maintenance planning problem for a numerous leased workstations. To satisfy the random demand and minimize the costs of production and maintenance, we establish a best combination between the variation of machines number, the production rates (as well as normal and over time planning of work) for each leased workstation, the inventory level and the returned products and we determine the optimal strategy maintenance characterising by the optimum number of preventive maintenance actions for all leased machines by showing the impact of production rates on the degradation degree of equipment's and consequently on the average number of failure.

  Fig. 1. Problem Description

  total production cost considering: the leasing cost; the installation and removal cost where the number of the machines varied from period to another; the cost of overtime work based on a binary variable θ k that equal to 1 when the quantity of demand at production period k surpasses the production quantity and all used machines M k work with upper bound normal time and equal to 0; the cost of inventory and unexploited capacities cost, is defined as follows:

Fig. 2 .

 2 Fig. 2. Total Maintenance cost according to T

Table III :

 III 1, is constant for all periods and the initial inventory level S 0 =0. The other data are given in sequence. Normal work time planning of each workstation

						Proceedings of the 2015 IEEE IEEM
	Using a numerical procedure method, an economically
	production plan and an optimal number of workstations
	are obtained and consequently the planning of normal
	time of production. The results are exhibited respectively
	in table II, III.
	Table II: Economical leasing machines and production plans
	k	k=1	k=2	k=3	k=4	k=5
	Mk	7	8	7	7	8
	Uk	11250 18250 12750 12750 19500
	Periods k	k=1	k=2	k=3	k=4	k=5
	W1	4	6	4	4	6
	W2	4	4	5	4	5
	W3	4	6	4	6	6
	W4	4	4	5	5	4
	W5	4	4	4	4	6
	W6	5	5	4	6	5
	W7	5	6	4	6	5
	W8	0	6	0	0	6
	W9	0	0	0	0	0
						c 1 =500 ; c 2 =0; c 3 =3.88 ; c 4 =2.42; c o =7 ; c n =5; c h =10 ;
						a 1 =250; a 2 =0 ;
						-τ r =1; δ =0.1; u=15
						-: lower bounds m=6 machines; upper bounds M=9
						workstations; upper bound of normal time work max N X	=6;
						and over time max S X	=2;
						-Probabilistic index (α=0.9).
						The input data concerning the average demand is listed in
						tables I
						Table I: Average of stationary demand
						1 d	d	2	d	3	d	4	d	5
						2286	22853	11880	15123	20653

978-1-4673-8066-9/15/$31.00 ©2015 IEEE

Proceedings of the 2015 IEEE IEEM


Sébastien Rohais
email: sebastien.rohais@ifpen.fr

Bernard Colletta

Isabelle Moretti

Pre-salt to salt stratigraphic architecture in a rift basin: insights from a basin-scale study of the Gulf of Suez (Egypt)

INTRODUCTION

Understanding the geology of extensional basins has a major economic impact as more than a third of the global hydrocarbon resources are hosted in rift basins [START_REF] Mann | Tectonic setting of the world's giant oil and gas fields[END_REF]. Rift basins have even faced a renewed interest during the 2000's with the increase in quality of seismic data resulting in huge discoveries from some rift systems below the salt along Brazilian and African margins [START_REF] Martin | Hunting the pre-salt. Frontier Exploration[END_REF][START_REF] O'reilly | Comparing the Brazilian and Angolan Conjugate Margin[END_REF].

Additionally, if rifts record generally the initial stage of crustal extension they occurred in a wide diversity of tectonic settings ranging from cratonic to orogenic belts settings. Rift basins have then been studied to address many scientific challenges such as the stretching of the continental lithosphere (e.g. [START_REF] Mckenzie | Some remarks on the development of sedimentary basins[END_REF][START_REF] Wernicke | Uniform-sense normal simple shear of the continental lithosphere[END_REF]Sleekler 1986;[START_REF] Moretti | The evolution of the Suez rift: a combination of stretching and secondary convection[END_REF], fault dynamics (e.g. [START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Colletta | Longitudinal evolution of the Suez rift structure (Egypt)[END_REF][START_REF] Moustafa | Internal structure and deformation of an accommodation zone in the northern part of the Suez rift[END_REF][START_REF] Gawthorpe | Linked sequence stratigraphic and structural evolution of propagating normal faults[END_REF][START_REF] Gupta | A. mechanism to explain rift basin subsidence and stratigraphic patterns through fault array evolution[END_REF][START_REF] Cowie | Implications of fault array evolution for syn-rift depocentre development: insights from a numerical fault growth model[END_REF][START_REF] Jackson | Growth and linkage of the East Tanka fault zone, Suez rift: structural style and syn-rift stratigraphic response[END_REF][START_REF] Khalil | Extensional fault-related folding, northwestern Red Sea, Egypt[END_REF] and the tectonic, sedimentation and erosion relationship (e.g. [START_REF] Leeder | Sedimentary models for extensional tilt-block/halfgraben basins[END_REF][START_REF] Garfunkel | Relation between continental rifting and uplifting: evidence from the Suez rift and northern Red Sea[END_REF][START_REF] Montenat | Tectonic and sedimentary evolution of the Gulf of Suez and the Northwestern Red Sea[END_REF][START_REF] Gawthorpe | Evolution of Miocene footwall derived coarsegrained deltas. Gulf of Suez, Egypt: implications for exploration[END_REF][START_REF] Lambiase | Structural controls on sedimentation in continental rifts[END_REF][START_REF] Bosence | Architecture and depositional sequences of Tertiary fault-block carbonate platforms; an analysis from outcrop and computer modelling[END_REF][START_REF] Bosworth | Structure, sedimentation, and basin dynamics during rifting of the Gulf of Suez[END_REF][START_REF] Gupta | Role of fault interactions in controlling synrift sediment dispersal patterns: Miocene Abu Alaqa Group. Suez Rift, Sinai, Egypt[END_REF]Rohais et al. 2007a;[START_REF] Omran | Tectonic evolution of the Southern Gulf of Suez, Egypt: a comparison between depocenter and near peripheral basins[END_REF]. Since the 80's and the recognition of the key role of surficial extensional structures and the deeper mantle thermal state, many scientific works were addressed to understand the relationship between the subsidence, or more generally the vertical movements, and the extension during the rift phases. The initial model of [START_REF] Mckenzie | Some remarks on the development of sedimentary basins[END_REF] emphased the role of lithospheric and crustal thinning and especially the post-rift thermal evolution of the upper mantle to qualify the post-rift subsidence. This post-rift subsidence is slow since it is mainly a thermal readjustment and is controlled by the conductivity of the mantle. At that time, discussions were still ongoing on the possibility of having fast crustal thinning induced by deep thermal anomaly or by far field extensional stresses (active versus passive rifting debate). It has then been proven that the crustal and lithospheric thinning can be fast enough to fit with the data which show extension may happen in just a few millions of years by taking into account a realistic rheology for the mantellic and crustal rock (e.g. [START_REF] Fleitout | Steady State secondary convection beneath lithospheric plates with temperature and pressure dependent viscosity[END_REF]. In these purely active rifting models, the crustal extension is only due to the deep thermal asthenosphere anomaly however the far field stresses, that could be or not extensive, influence the resulting rift geometry as proposed by [START_REF] Moretti | Thermomechanical models of active rifting[END_REF]. The difference between the amount of upper crustal extension (Extc) and crustal thinning (c) has also been recognized for a long time, since deep seismic profiles have been acquired. c is always bigger than Extc and this difference was classically interpreted by the authors, in the active rift scheme, in term of different rheologies: brittle upper crust and ductile lower crust [START_REF] Moretti | Discrepancy between lower and upper crustal thinning. In Sedimentary basins and basin-forming mechanisms[END_REF]. However, based also on the first deep seismic acquisitions, it has been noticed that the localization of the maximum of the crustal thinning may not correspond to the maximum of extension in the upper crust and proposed crustal-scale fault (i.e. rather brittle lower crust, [START_REF] Wernicke | Uniform-sense normal simple shear of the continental lithosphere[END_REF]. Meanwhile, data from basins where the subsidence is huge compare to the upper crustal extension suggested that gravity anomalies induced by phase change in the lower crust may also induce subsidence without any far field extension or mantellic thermal anomaly [START_REF] Sleep | Platform basins[END_REF]Artyushkov and Baer, 1984). Later the works of Huysman (1999) have proven that the "future" of any passive rift is an active one since the destabilization of the lithosphere/asthenosphere boundary is sufficient to start a mantellic convective cell that will speed up the lithospheric thinning. The common characteristic of all these proposals to explain rifting, which are not contradictory as all extensional areas have not necessarily the same origin, is that they neglect the effect of the surface processes on the rift evolution. The recognition of the coupling between erosion/sedimentation and deep processes has been facilitated for the last 15 years by the improvement of softwares used to model the lithospheric evolution. This improvement now allows us not only to compute isostatic rebound related to erosion or subsidence due to sediment load, but also to quantify how the upper crustal loading/unloading may influences the mantellic state [START_REF] Burov | Erosion and rheology controls on syn-and post-rift evolution: Verifying old and new ideas using a fully coupled numerical model[END_REF][START_REF] Haines | INDEPTH III seismic data: From surface observations to deep crustal processes in Tibet[END_REF][START_REF] Cloetingh | Coupled Deep Earth and surface processes and their impact on geohazards[END_REF]. One of the key objectives at present is establishing the relationship between deep and surface processes; how does subsidence / extension / uplift / erosion interact all along a rift history? A major limitation preventing the implementation and optimization of these numerical models is the lack of a well constrained case study. A better calibration of theoretical concepts to real data observations is essential to deliver applicable results. Synthetic overviews have been proposed for the evolution from rifting (e.g. [START_REF] Chaboureau | Paleogeographic evolution of the central segment of the South Atlantic during Early Cretaceous times: paleotopographic and geodynamic implications[END_REF][START_REF] Macgregor | History of the development of the East African Rift System: A series of interpreted maps through time[END_REF] up to oceanic spreading (e.g. [START_REF] Leroy | From rifting to oceanic spreading in the Gulf of Aden: a synthesis[END_REF]. However, the time step and depositional system description do not provide enough resolution to constrain, at high resolution, the evolution of a full rift system from its initiation to late rift stages.

The present contribution proposes a basin-scale study of a rift basin resulting in a geological scenario including its timing, depocenter migration, depositional system evolution and erosion-sedimentation relationship. The Suez rift has been selected to address this topic as it provides a well constrained geological setting with high resolution dating constraints and a large quantity of accessible and diversified data from both outcrop and subsurface. This study is focused on the pre-salt to salt series of the Suez rift that correspond to Oligo-miocene synrift deposits recording the rift initiation to the latest rift phases.

SUEZ RIFT: GEOLOGIC BACKGROUND AND BASIN SETTING

The Suez rift is the NW-SE-trending branch of the Red Sea rift system (Figure 1), resulting from the late Oligocene to early Miocene rifting of the African and Arabian plates [START_REF] Garfunkel | The tectonics of the Suez rift[END_REF]. It is bounded on both margins by large-scale normal fault zones (fault length ~40-80 km, fault throw ~2-6 km). The polarity of the block-bounding faults changes along the axis of the rift, dividing the rift into three 50-100 km long tectonic domains [START_REF] Colletta | Longitudinal evolution of the Suez rift structure (Egypt)[END_REF][START_REF] Patton | Tectonic evolution and structural setting of the Suez Rift[END_REF][START_REF] Moustafa | Internal structure and deformation of an accommodation zone in the northern part of the Suez rift[END_REF]): (1) the northern Darag basin with southwest dips; (2) the Central basin (Belayim province) with northeast dips; (3) the Southern basin (Amal-Zeit province) with southwest dips (Figure 1a). In between, two major ca. 20-km wide accommodation zones exist [START_REF] Colletta | Longitudinal evolution of the Suez rift structure (Egypt)[END_REF]): the Zaafarana and the Morgan accommodation zones (Figure 1a).

The stratigraphic succession of the Gulf of Suez includes pre-rift and syn-rift successions (Figure 1c). The pre-rift succession is presented hereafter as it constitutes the catchment unit feeding the syn-rift depositional systems. It comprises a Precambrian Pan-African crystalline basement unconformably overlain by a 1-km thick succession of Cambrian to Eocene sedimentary rocks that progressively thins toward the south. This sedimentary succession can be subdivided into three distinct units (e.g. [START_REF] Moustafa | Block faulting in the Gulf of Suez[END_REF][START_REF] Garfunkel | The tectonics of the Suez rift[END_REF]: (1) the "Nubia Sandstones" corresponding to several formations which mostly consist of fluvial sandstones (Cambrian to Early Cretaceous), (2) a Late Cretaceous mixed carbonate-siliciclastic succession and (3) a Paleocene-Eocene carbonate-dominated succession (Figure 1c).

The transition from pre-rift to syn-rift is locally recorded by red bed deposits overlying a major angular unconformity (Figure 1c). They correspond to the Tayiba and Abu Zenima Formations (Figure 1c) that are commonly attributed to the Oligo-Miocene. This date is based on interbedded basaltic flows and/or volcanic material found within these formations, which absolute K-Ar ages span from 21 to 27 Ma (e.g. [START_REF] Montenat | Tectonic and sedimentary evolution of the Gulf of Suez and the Northwestern Red Sea: a review[END_REF][START_REF] Plaziat | Stratigraphy of the Egyptian syn-rift deposits: correlations between axial and peripheral sequences of the north-western Red Sea and Gulf of Suez and their relations with tectonics and eustacy[END_REF].

The syn-rift Miocene succession is subdivided into the Gharandal Group consisting of the Nukhul, Rudeis and Kareem Formations, and the Ras Malaab Group consisting of the Belayim, South Gharib and Zeit Formations (e.g. EGPC 1964; Figure 1c, Figure 2). The post-Zeit succession includes the Wardan and Zaafarana Formations (Figure 2), attributed to the Plio-Pleistocene (e.g. Abd [START_REF] Shafy | Miocene-Pliocene boundary in the Gulf of Suez region, Egypt. 10th EGPC Exploration Seminar[END_REF]). The post-Zeit deposits are not presented in this paper as they correspond to post-rift deposits (Figure 1c).

The Nukhul Formation is Aquitanian-Early Burdigalian in age (e.g. [START_REF] Garfunkel | The tectonics of the Suez rift[END_REF][START_REF] Fawzy | Regional study of Miocene evaporates and Pliocene-recent sediments in the Gulf of Suez[END_REF][START_REF] Scott | Early depositional history of a rift basin: Miocene in western Sinai[END_REF] and is subdivided into a basal Shoab Ali Member and other three time equivalent members: the Ghara, October and Gharamul Members (Saoudi and Khalil 1984, Figure 2). The Nukhul Formation includes sabkha-type evaporites (anhydrite) and shales, marginal to shallow-marine calcareous conglomerates, reefs and platform carbonates, sandstones, marls and deep marine shales (e.g. [START_REF] Ghorab | Oligocene and Miocene rock stratigraphy of the Gulf of Suez region, unpublished report consultatus stratigraphic committee of the EGPC[END_REF]Hughes et al. 1992).

The Rudeis Formation is Burdigalian to Early Langhian in age (e.g. [START_REF] Bunter | Tectonic control on carbonate platform facies distribution and sequence stratigraphy: Miocene, Gulf of Suez[END_REF][START_REF] Smale | Sedimentologic evidence for early Miocene fault reactivation in the Gulf of Suez[END_REF]Hughes et al. 1992) and is generally subdivided into several members that are commonly grouped into a Lower Rudeis and an Upper Rudeis units (EGPC 1964, Figure 2).

The boundary between them is defined by a sharp limit and facies change recording a basinward shift [START_REF] Garfunkel | The tectonics of the Suez rift[END_REF]. The Rudeis Formation includes widespread, offshore marly/shaly deposits with thin sandstone beds (Lower Rudeis) interpreted as turbidite and debris flow deposits and coarse-grained fan-delta conglomerates with interbedded marls and siltstones (Upper Rudeis) [START_REF] Ghorab | Oligocene and Miocene rock stratigraphy of the Gulf of Suez region, unpublished report consultatus stratigraphic committee of the EGPC[END_REF]. The Rudeis Formation also includes shallow marine reefal carbonates developed along isolated tilted block crests (Burchette 1987; [START_REF] Bosence | Architecture and depositional sequences of Tertiary fault-block carbonate platforms; an analysis from outcrop and computer modelling[END_REF].

The Kareem Formation is Langhian in age (e.g. [START_REF] Garfunkel | The tectonics of the Suez rift[END_REF][START_REF] Allen | Subsurface sedimentological study of the Rudeis Formation in Kareem, Ayun, Yusr and Shukheir fields[END_REF] and is subdivided into a basal Markha Member (equivalent to Rahmi Member) and an upper Shagar Member (EGPC, 1964, Figure 2). The Markha Member mainly includes thin anhydrite beds interbedded with shale, marls and carbonates. The Shagar Member includes shallow marine carbonates and sandstones to deep-water marls and dark grey shales [START_REF] Ghorab | Oligocene and Miocene rock stratigraphy of the Gulf of Suez region, unpublished report consultatus stratigraphic committee of the EGPC[END_REF].

The Belayim Formation is Serravallian in age (e.g. [START_REF] Bunter | Tectonic control on carbonate platform facies distribution and sequence stratigraphy: Miocene, Gulf of Suez[END_REF][START_REF] Scott | Early depositional history of a rift basin: Miocene in western Sinai[END_REF] and includes four members: the Baba, Sidri, Feiran and Hammam Faraun Members (EGPC 1964).

The Belayim Formation consists of alternating halite, anhydrites, siliciclastics and reef carbonates composed of red-algae (Nullipore limestone defined by [START_REF] Sellwood | Facies evolution in the Gulf of Suez area: sedimentation history as an indicator of rift initiation and development[END_REF] recording a wide spectrum of depositional environments from lagoonal and shallow platform to deep marine (Figure 2).

The South Gharib Formation is Serravallian to Tortonian (e.g. [START_REF] Bunter | Tectonic control on carbonate platform facies distribution and sequence stratigraphy: Miocene, Gulf of Suez[END_REF][START_REF] Scott | Early depositional history of a rift basin: Miocene in western Sinai[END_REF][START_REF] Smale | Sedimentologic evidence for early Miocene fault reactivation in the Gulf of Suez[END_REF], Figure 2) and consists of massive halite and thin anhydrite beds interbedded with fine-grained sandstones and shales associated to an alternation of restricted hypersaline environments with moderately deep to shallow marine environments (Hughes et al. 1992;[START_REF] Rouchy | Evaporitic and biosiliceous cyclic sedimentation in the Miocene of the Gulf of Suez-depositional and diagenetic aspects[END_REF].

The Zeit Formation is Messinian (e.g. [START_REF] Bunter | Tectonic control on carbonate platform facies distribution and sequence stratigraphy: Miocene, Gulf of Suez[END_REF][START_REF] Scott | Early depositional history of a rift basin: Miocene in western Sinai[END_REF][START_REF] Zierenberg | Isotopic constraints on the origin of the Atlantis II, Suakin and Valdivia brines, Red Sea[END_REF][START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF] and consists of halite, gypsum, anhydrite beds interbedded with fine-grained sandstones, siltstones and shales associated to shallow marine

The workflow developed hereafter includes firstly a structural map interpretation and synthesis based on new fieldwork and previous published works (Figure 1). Secondly, sequence stratigraphic correlation has been carried out using 279 wells and 31 sedimentological outcrop sections distributed all over the basin (Figure 1). We refer to the stratigraphic surfaces based on the published microfossils and data following the synthesis by [START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF], Hughes et al. (1992) and El [START_REF] El Beialy | Insights on the age, climate and depositional environments of the Rudeis and Kareem formations, GS-78-1 well, Gulf of Suez, Egypt: A Palynological Approach[END_REF] (Figure 2). These surfaces have been correlated all over the basin along several longitudinal and dip cross sections (Figure 3). We then calibrated these stratigraphic ages into absolute ages using the ICS ( 2004) stratigraphic chart based on the synthesis by [START_REF] Ghorab | Oligocene and Miocene rock stratigraphy of the Gulf of Suez region, unpublished report consultatus stratigraphic committee of the EGPC[END_REF] (Figure 2).

The pioneer work done by Hughes et al. (1992) has also been used to subdivide the stratigraphic period at higher resolution than the formation subdivision to be compatible with their microfaunal assemblage zones (B1-4, K1-2, R1-5, Nu1-3; Figure 2). We also refer to the work by [START_REF] Krebs | Graphic correlation and sequence stratigraphy of Neogene rocks in the Gulf of Suez. In Fauna, flora and sequence stratigraphy[END_REF] and [START_REF] Wescott | Modern applications of biostratigraphy in exploration and production[END_REF] for the sequence labeling (Figure 2). Thirdly, lithologic maps have been established (Figure 4) using sequence stratigraphic correlation and interpreted using constrains from paleoenvironmental data (Hughes et al. 1992;[START_REF] El Beialy | Insights on the age, climate and depositional environments of the Rudeis and Kareem formations, GS-78-1 well, Gulf of Suez, Egypt: A Palynological Approach[END_REF]) and previous published maps (Nuhkul Fm: Saoudi and Khalil 1984;[START_REF] Khaled | Rift architecture and growth sedimentation across a main accommodation zone, Northern Gulf of Suez -Egypt[END_REF]Peijs et al. 2012, Rudeis Fm: Hagras and[START_REF] Hagras | Sand distribution of Miocene clastics in the Gulf of Suez[END_REF]Hughes et al. 1992;[START_REF] Schütz | Structure and stratigraphy of the Gulf of Suez, Egypt[END_REF][START_REF] Bosworth | Structure, sedimentation, and basin dynamics during rifting of the Gulf of Suez[END_REF][START_REF] Gawthorpe | Fault growth, interaction, linkage and death: evolution of the Hammam Faraun fault block, Suez rift, Egypt[END_REF][START_REF] Peijs | The Gulf of Suez rift basin[END_REF], Kareem Fm: Hughes et al. 1992;[START_REF] Schütz | Structure and stratigraphy of the Gulf of Suez, Egypt[END_REF][START_REF] Salah | The Miocene Kareem Formation in the southern Gulf of Suez, Egypt: a review on stratigraphy and petroleum geology[END_REF][START_REF] Khaled | Rift architecture and growth sedimentation across a main accommodation zone, Northern Gulf of Suez -Egypt[END_REF][START_REF] Peijs | The Gulf of Suez rift basin[END_REF], Belayim Fm: Khaled et al. 2002, South Gharib/Zeit Fms: Richardson and Arthur 1988). To keep the maps readable, we have only highlighted the deepest part of the basin using the paleo-bathymetry constrains from Hughes et al. (1992). Three main bathymetric ranges were used with: moderately to deep environments (30-100 m in paleo-bathymetry), deep environments (100-200 m in paleo-bathymetry) and very deep environments (> 200 m in paleo-bathymetry) (Figure 2, Figure 4). As a result, nineteen lithological maps are presented over an updated structural framework. A step by step structural restoration was beyond the scope of this study. Indeed, structural restoration and backstripping need as inputs some idea of the paleogeography such as sea floor geometry and eroded thicknesses. In a complex area with contrasted reliefs as the Gulf of Suez, the facies and the lateral variations of these facies are the better indicators of these paleogeographies. As a result the 3D restoration cannot be done before the analysis presented here. All the maps are thus shown over the present day structural framework (Figure 4). Fourthly, isopach / depocenter maps have been established (Figure 5) based on wells and outcrop sections as well as the previous published works using in-house 3D geological modeling tools [START_REF] Barrois | Coupling 3D Structural Restoration with Stratigraphic Modelling in Rifted Margins, Suez Rift, Egypt. International conference "Modelling sedimentary basins and their petroleum systems[END_REF]Barrois 2011).

Finally, mean sediment supply, mean carbonate accumulation rate and mean evaporite accumulation rate were computed from these 3D database (Table 1) using the same methodology proposed by [START_REF] Poag | A record of Appalachian denudation in Post-Rift Mesozoic and Cenozoic sedimentary deposits of the U.S. Middle Atlantic Continental margin[END_REF], [START_REF] Rouby | Sediment supply to the Orange sedimentary system over the last150 My: an evaluation from sedimentation/denudation balance[END_REF] and [START_REF] Guillocheau | Quantification and causes of the terrigeneous sediment budget at the scale of a continental margin: a new method applied to the Namibia-South Africa margin[END_REF]. For each time step, we computed the relative proportion of the lithologies using an automatic image analysis based on the lihtologic maps. The six dominant lithologies have then been gathered into groups to be able to compute an accumulation rate for evaporites (anhydrite and halite), carbonates (carbonates and offshore mudstones) and sediment supply form siliciclastic deposits (shales, sandstones, conglomerates). An optimist, pessimist and preferred scenario have been established to explore the maximum and minimum development for each group of lithology depending on the drawing and extrapolation on the maps (Evaporites, Carbonates and Siliciclastics; Table 1). The preferred scenario corresponds to the lithologic maps presented in Figure 4. Then we estimated the volume for each group of lithology by modulating these relative proportions to the volume of preserved sediment for each time steps (Table 1). Carbonate volumes have been corrected with a porosity of 10% and siliciclastic volumes with 20% (e.g. [START_REF] Rouby | Sediment supply to the Orange sedimentary system over the last150 My: an evaluation from sedimentation/denudation balance[END_REF][START_REF] Guillocheau | Quantification and causes of the terrigeneous sediment budget at the scale of a continental margin: a new method applied to the Namibia-South Africa margin[END_REF]. A minimum and maximum have also been computed to established error bar on the accumulation rates as well as on the sediment supply (Table 1) and are presented in Figure 6.

STRATIGRAPHIC ARCHITECTURE AND PALEOGEOGRAPHY

Stacking pattern has been used to correlate the main surfaces at basin-scale and then to characterize the distribution of the main syn-rift formations (Figure 2, Figure 3). The identification of the main facies, environment of deposition (EOD) and depositional profiles is based on the solid sedimentological and environmental knowledge provided by previous studies (e.g. Burchette, 1987;[START_REF] Montenat | Tectonic and sedimentary evolution of the Gulf of Suez and the Northwestern Red Sea[END_REF][START_REF] Gawthorpe | Evolution of Miocene footwall derived coarsegrained deltas. Gulf of Suez, Egypt: implications for exploration[END_REF]Hughes et al. 1992;[START_REF] Rouchy | Evaporitic and biosiliceous cyclic sedimentation in the Miocene of the Gulf of Suez-depositional and diagenetic aspects[END_REF][START_REF] Salah | The Miocene Kareem Formation in the southern Gulf of Suez, Egypt: a review on stratigraphy and petroleum geology[END_REF][START_REF] Bosence | Architecture and depositional sequences of Tertiary fault-block carbonate platforms; an analysis from outcrop and computer modelling[END_REF][START_REF] Gupta | Role of fault interactions in controlling synrift sediment dispersal patterns: Miocene Abu Alaqa Group. Suez Rift, Sinai, Egypt[END_REF][START_REF] Young | Sedimentology and sequence stratigraphy of a transfer zone coarse-grained delta, Miocene Suez Rift, Egypt[END_REF][START_REF] Winn | Lower Miocene Nukhul Formation, Gebel el Zeit, Egypt: Model for structural control on early synrift strata and reservoirs, Gulf of Suez[END_REF][START_REF] Jackson | Normal faulting as a control on the stratigraphic development of shallow marine syn-rift sequences: the Nukhul and Lower Rudeis Formations, Hammam Faraun fault block, Suez Rift, Egypt[END_REF][START_REF] El-Naby | Sequence-stratigraphic interpretation of structurally controlled deposition: Middle Miocene Kareem Formation, southwestern Gulf of Suez, Egypt[END_REF]; Omran and El Sharawy 2014; Figure 2). Stratigraphic architecture has then been restored by interpreting the sequences using six dominant lithologies: carbonates (including reef and platform s.l. deposits), shales (silty rich from protected to restricted deposits, versus mud rich for offshore deposits), sandstones (including fan delta, shallow marine and turdiditic deposits), conglomerates (including alluvial fan and fan delta deposits), anhydrite and halite (mainly from lagoon and saline to sabkha depositional settings). (Miocene,~Aquitanian, The timeframe defined by Hughes et al. (1992) has been used to establish three key phases during the Nukhul Fm deposition (N1 to N3, each of which lasted ca. 0.9 Myr). The main hypothesis for the paleogeographic restoration was that the Shoab Ali Mb was time equivalent to Nukhul Fm deposits in the northern part of the rift, a consistent interpretation with the [START_REF] Bosworth | Structural and stratigraphic evolution of the Gulf of Suez rift, Egypt: a synthesis[END_REF] review. The Nukhul Fm recorded a progressive flooding from the Mediterranean Sea (Figure 4a-c) with a progressive evolution from supra-littoral to moderately deep depositional environments (paleo-bathymetry 30-100 m). Large scale tectonic structures (e.g. accommodation zone, Darag, Central and Southern basins) as well as small scale structures (e.g. tilted block crest, hanging-wall and relay ramp) clearly had an influence onto facies distribution and partitioning (Figure 4a-c). The tilted block crests are commonly surrounded by shallow carbonate deposits while in the hanging-wall setting siliciclastic dominated deposits mainly occurred especially in the Central and Southern basins (Figure 4a-c).

Nukhul Formation

Nu3 (ca. 22.1-23Ma)

The Darag, Central and Southern basins were individualized in terms of depositional environments (Figure 4a). To the south, the Southern basin was characterized by siliciclastic dominated deposits with alluvial fan and fluvio-lacustrine depositional environments. The Morgan accommodation zone was mainly sub-aerial and starved of sediment (Figure 4a). The Central basin was characterized by mixed deposits with shallow marine to restricted deposits.

The Zaafarana accommodation zone was characterized by shallow marine deposits recording the transition toward open marine setting to the north (Figure 4a). The Darag basin was thus mainly characterized by open marine deposits (Figure 4a).

Nu2 (ca. 21.2-22.1Ma)

The Darag, Central basins were still individualized in term of depositional environments from the Southern basin showing a N-S depositional gradient (Figure 4b). The marine flooding from the Mediterranean Sea reached the Central basin. The input of siliciclastics decreased relatively to the south in comparison with Nu3. The depositional profile includes carbonate platforms and isolated reefs along tilted block crests and submerged paleohighs facing moderate to deep basinal marine shales (Darag and Central basins, Figure 4b). The Southern basin was characterized by lagoon deposits and marginal marine sabkha evaporites (Figure 4b). There was no clear evidence that the marine flooding originated from the Red Sea to the south. The overall flooding coming from the Mediterranean Sea progressively reached the Morgan accommodation zone (Figure 4c). Deep marine sediments were deposited in the Darag basin (Figure 4c). The input of siliciclastics became progressively localized along the future rift shoulders. Evaporites were preserved in isolated ponds from marginal marine systems in the Southern basin (Figure 4c). There was still no evidence that marine flooding originated from the Red Sea. (Miocene,~Burdigalian, The periods of time defined by Hughes et al. (1992) has been used to establish four key phases during the Rudeis Fm deposition (R5, R3, R2 and R1). The Rudeis Fm recorded the flooding from both the Mediterranean Sea and the Red Sea and their connection (Figure 4dg). It has recorded the deepest depositional environments (> 200 m in bathymetry) and a least four main anoxic events (Hughes et al. 1992; Figure 2). Large and small scale tectonic structures influenced facies distribution and partitioning (Figure 3). While during the Nukhul R5 The Rudeis Fm was strongly transgressive onto the Nuhkul Fm with several onlap features indicating a widening of the depocenters (Figure 3). Very deep (200-400 m deep) open marine conditions occurred all along the basin axis with local anoxia (Hughes et al., 1992, Figure 4d). It was the very first time that a marine connection occurred between the Mediterranean Sea and the Red Sea (Figure 4d). The input of siliciclastics was mainly localized along the rift shoulders and most of the tilted block crests were progressively onlapped by carbonate reefs and platforms (Figure 4d). Sandstones were locally delivered to the basin axis throughout the main accommodation zones (Morgan and Zaafarana) and smaller relay ramp areas (e.g. Baba-Belayim area, Figure 4d). The R5 period of time is interpreted as the overall maximum flooding event during the rift evolution (Figure 2).

Nu1

Rudeis Formation

R3 (ca. 17.6-18.5 Ma)

The trend initiated during the previous stage continued with very deep open marine conditions all along the basin axis and input of siliciclastics along the rift shoulders (Figure 4e). The R3 period of time recorded the widest spread and thickest distal offshore deposits (Figure 4e), with very deep (200-400 m deep) open marine conditions characterized by another major anoxic event (Hughes et al., 1992; Figure 2). The R2 period of time (equivalent to the basal portion of the Upper Rudeis) marked a major change during the rift evolution (Figure 4f), traditionally related to the mid-Clysmic event [START_REF] Garfunkel | The tectonics of the Suez rift[END_REF]. A major increase in the sediment supply from the eastern rift shoulder was recorded by large and very coarse-grained fan deltas (Figure 4f). The basin axis also recorded a major pulse in siliciclastics (Figure 4f). The isolated platforms developed along tilted block crests were characterized by thickening and widening trends suggesting a relative imbalance of production rate over the accommodation space. This could be interpreted as a progressive subsidence of the tilted block crests. Short duration anoxic events could have locally occurred (Hughes et al. 1992; Figure 2). The R2 period of time marked the transition toward an overall forced regressive trend at rift scale that was recorded by the Upper Rudeis, Kareem and Belayim Formations (Figure 2).

R2

R1 (ca. 15.8-16.7Ma)

The forced regressive trend initiated during the previous stage continued (Figure 4g). The R1 period of time recorded the last major anoxic event during the rift evolution (Hughes et al. 1992; Figure 2). A progressive decrease in paleo-bathymetry and a change in sea bottom conditions have been inferred from the benthonic foraminifera assemblages (Hughes et al. 1992; Figure 2). The R1 deposits are organized in an overall prograding trend up to the first major sequence boundary (T30, boundary between Rudeis and Kareem Formations) recorded at basin-scale (e.g. Figure 3d, massive sandstone package organized in a forced regressive trend along well 47). (Miocene,~Langhian, We mainly refer to the work done by Hughes et al. (1992), [START_REF] Salah | The Miocene Kareem Formation in the southern Gulf of Suez, Egypt: a review on stratigraphy and petroleum geology[END_REF] and El [START_REF] Beialy | Dinoflagellates from the Miocene Rudeis and Kareem formations borehole GS-78-1, Gulf of Suez, Egypt[END_REF] to establish four key phases during the Kareem Fm deposition (Figure 4hk). The Kareem Fm recorded the progressive disconnection between the Mediterranean Sea and the Red Sea (Figure 4h-k). Deep to very deep water depositional environments were developed (> 200 m in bathymetry), nevertheless, the Kareem Fm constitutes a transition toward mainly oxic paleoenvironmental conditions (Hughes et al. 1992; Figure 2). Large scale tectonic structures had a major influence onto facies distribution and partitioning (Figure 4hk). As for the previous period of time (Rudeis Fm), siliciclastics were mainly preserved in the Southern basin, Morgan accommodation zone and along the rift bounding faults. The K2basal Markha deposits overlaid a major sequence boundary (T30 ca. 15.8 Ma; Figure 2, Figure 3). Open marine conditions still prevailed in the northern part of the rift (Darag basin and Zaafarana accommodation zone) and the southernmost part (SE of the Southern basin). Very large carbonate platforms occurred in the Southern basin and along the Zaafarana accommodation zone (Figure 4h). The Central basin was characterized by large and thick anhydrite deposits laterally passing to shallow marine carbonates to the north and to the south east (Figure 4h). This paleogeographic configuration thus recorded the first evidence during the syn-rift deposition of disconnection between the Mediterranean Sea and the Red Sea (Figure 4h). Rift shoulders still constituted the main source areas for siliciclastics (Figure 4h). The K2 -Middle Markha deposits recorded a new major flooding from both the Mediterranean Sea and the Red Sea (Figure 4i). Depositional environments and lithology distributions were very similar to those occurring during the deposition of the R3-Rudeis Fm deposits with neither evidences of anoxic nor suboxic conditions (Figure 2) as paleobathymetry was relatively lower (Figure 4i). K2/K1 transition -Markha/Shagar (ca. 14. The K2/K1 transition -Markha/Shagar deposits recorded another major disconnection between the Mediterranean Sea and the Red Sea. As for the K2basal Markha deposits, open marine conditions only prevailed in the northern part and the southernmost part of the Suez rift (Figure 4j). The Zaafarana accommodation zone controlled the occurrence of a large carbonate platform recording the transition from open marine setting to the north to a restricted setting in the Central basin (Figure 4j). The K1 -Top Shagar deposits recorded a major flooding event occurring at basin-scale (Figure 4k). Isolated platforms were very small and restricted to tilted block crests (Figure 4k). Siliciclastic were mainly derived from the rift shoulders, especially in the Southern basin and along the Morgan accommodation zone (Figure 4k). The topmost part of K1 -Top Shagar deposits are organized in an overall prograding trend up to the second major sequence boundary recorded at basin-scale (T50 ca. 13.6 Ma; Figure 2, Figure 3). (Miocene,~Serravallian , The periods of time defined by Hughes et al. (1992) have been used to establish four key phases during the Belayim Fm deposition (B4, B3, B2 and B1). The Belayim Fm recorded a progressive disconnection between the Mediterranean Sea and the Red Sea in the Suez rift (Figure 4l-o). It has recorded the first thick and widely distributed salt deposits over the Suez rift (Figure 3, Figure 4l). The Belayim Fm also illustrates the full depositional profile from open marine setting in the south (Southern basin) to restricted environments with a lateral facies change from anhydrite to halite in the north (Darag basin, Figure 4l andn). Small scale tectonic structures had influence onto facies distribution (e.g. faulted controlled depocenters with halite on Figure 4l). The input of siliciclastic was mainly localized along the Morgan accommodation zone and in the Central basin (Figure 4l-o). Ma)

Kareem Formation

K2basal

K2 -Middle

K1 -Top

Belayim Formation

The B4 -Baba deposits recorded the first disconnection of the entire Suez rift from the Mediterranean Sea and an overall restriction of the Darag, Central and Southern basins (Figure 4l). Halite deposits were preserved in fault controlled depocenters (Figure 4l).

Sediment supplies along the rift shoulders were very low as suggested by the very small isolated siliciclatics bodies (e.g. Wadi Araba, Belayim and Baba areas; Figure 4l). A large carbonate platform was developed to the south of the Southern basin, recording the transition toward more open marine setting in the Rea Sea to the south (Figure 4l).

B3 -Sidri (ca. 12.6-13.1 Ma)

The B3 -Sidri deposits (as the top Shagar) recorded one of the last flooding events occurring at basin-scale in the Suez rift (Figure 4m). The Southern basin was characterized by a restricted environment along its western part (Zeit area), while open marine conditions prevailed along a north to south corridor to the east (Figure 4m). Siliciclastic supplies were mainly localized in the Central basin and along the Morgan accommodation zone where the Precambrian basement was denudated (Figure 4m).

B2 -Feiran (ca. 12.1-12.6 Ma)

The B3 -Feiran deposits recorded a second full disconnection from the Mediterranean Sea as the B4 -Baba deposits (Figure 4n). Halite deposits were preserved in fault controlled depocenters in the Southern basin and along the Morgan accommodation zone suggesting less intense evaporation processes in the Central basin compared to the B4 -Baba period of time (Figure 4l). Very small isolated siliciclatics bodies were preserved especially in the Wadi Araba, Belayim and Baba areas (Figure 4n). As for the B4 -Baba deposits, a large carbonate platform was developed to the south of the Southern basin (Figure 4n). The B1 -Hammam Faraun deposits recorded the very last marine flooding event occurring at basin-scale connecting the Mediterranean Sea and the Red Sea (Figure 4o). Paleogeographic setting was very similar to the B3 -Sidri period of time, with restricted and shallow environments in the Zeit area and isolated inputs of siliciclastics (Wadi Araba, Morgan Accommodation zone, Belayim and Baba areas; Figure 4o). The restricted depositional environments preserved to the east of the Darag basin and the open marine deposits to the north were the last sedimentary records before a long period of erosion and/or non-deposition to the north of the Suez rift (Figure 4o). Formation (Miocene,~Tortonian , No high resolution biostratigraphic constraints for the South Gharib Fm were available as the ones provided by Hughes et al. (1992) for the previous formations. We thus choose to highlight only two key phases during the deposition of the South Gharib Fm: its lowermost and uppermost parts. The three main basins were characterized by a north to south paleogeographic gradient with highly evaporitic setting to the south and more siliciclastic and mixed setting to the north (Figure 4p-q). Halite deposits were preserved in fault controlled depocenters (Figure 3, Figure 4p-q). The input of siliciclastic was spatially localized and almost corresponded to the present day feeding points (Figure 4p-q). Evaporation processes were the dominant sedimentary processes.

B1 -Hammam

South Gharib

Lower South The Lower South Gharib deposits overlaid a major sequence boundary (T60 ca. 11.8 Ma; Figure 2, Figure 3). For the very first time, anhydrite and halite deposits occupied the whole of the Suez rift (Figure 4p). Fault controlled depocenters characterized by halite deposits were connected into very large depocenters in the Southern basin up to the Morgan accommodation zone (Figure 4p). The Central basin and the Zaafarana accommodation zone were characterized by anhydrite deposits with fault controlled halite deposits, recording the transition toward the Darag basin where only condensed siliciclastic deposits were preserved (Figure 3, Figure 4p). There were no preserved deposits in the northern part of the Darag basin (Figure 3, Figure 4p).

Upper South Gharib (ca. 7.2-9.5 Ma)

The Upper South Gharib deposits were organized in a similar trend as the South Gharib deposits with highly evaporitic setting to the south (Figure 3, Figure 4q). The Southern and Central basins were characterized by fault controlled halite depocenters connected by very continuous anhydrite deposits (Figure 4q). The inputs of siliciclastics were localized along the main feeding points already active during the deposition of the Lower South Gharib (Figure 4q). The size of the fan systems was much larger than during the deposition of the Lower South Gharib suggesting an increase in the water supplies coming from the catchment areas (Figure 4q). (Miocene,~Messinian , As it happens for the case of the South Gharib Fm, no high resolution biostratigraphy was available for the Zeit Fm so it was subdivided into a lower and an upper part (Figure 4r-s).

Zeit Formation

The same paleogeographic gradient as for the South Gharib Fm deposition was identified with highly evaporitic setting to the south (Figure 3, Figure 4r-s). Halite and/or anhydrite deposits were preserved in fault controlled depocenters (Figure 4r-s). The input of siliciclastic was spatially localized and almost corresponds to the present day feeding points (Figure 4r-s).

Evaporation processes were still important, but the input of siliciclastics increased as well as mixed carbonate dominated deposits compared to the South Gharib period of time suggesting more humid climatic setting (Figure 3, Figure 4r-s).

Lower Zeit (ca. 6.2-7.2 Ma)

The Lower Zeit deposits recorded a period of relatively low occurrence of evaporate deposits during the Tortonian-Messinian time interval (Figure 4r). Small isolated evaporitic depocenters occurred in the Central and Darag basins mainly filled with anhydrite and few halite deposits (Figure 4r). The Southern basin was characterized by fault controlled halite small depocenters connected by very continuous anhydrite deposits (Figure 4r). Siliciclastic supplies were the highest during the Tortonian-Messinian time interval (Figure 6). There were no deposits preserved in the northern part of the Darag basin (Figure 3, Figure 4r).

Upper The Upper Zeit deposits recorded another pulse in evaporitic conditions, almost equivalent to the Upper South Gharib Fm in term of spatial distribution (Figure 4s). Two large fault controlled depocenters with halite were preserved in the Central basin. The Southern basin was still characterized by small fault controlled depocenters with halite and continuous anhydrite deposits (Figure 4s). Siliciclastic supplies were still high with large localized fan system (Figure 4s). No deposits from this age were preserved in the northern part of the Suez rift (Figure 4s).

RIFT DYNAMICS, SUBSIDENCE AND UPLIFT

The presented stratigraphic architecture restoration (Figure 3, Figure 4) has been then combined to thickness and depocenter maps analysis (Figure 5) and discussed in the light of the subsidence and uplift dynamics within the rift evolution taking into account the published subsidence analysis [START_REF] Steckler | Uplift and extension at the Gulf of Suez: indications of induced mantle convection[END_REF][START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Moretti | The evolution of the Suez rift: a combination of stretching and secondary convection[END_REF][START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF]; Figure 6). The total amount of uplift/exhumation during the rift evolution has been estimated to about 5-7 km on the western rift shoulder [START_REF] Omar | Fission-track analysis of basement apatites at the western margin of the Gulf of Suez rift, Egypt: evidence for synchronicity of uplift and subsidence[END_REF].

Rift initiation (Oligocene, ~Chattian. ca. 1-4Myr duration)

Faunas, stratigraphic relationships, K-Ar and Ar-Ar dates indicate that the onset of the rifting is no younger than 25-27 Ma in the Southern basin area (e.g. [START_REF] Shinnawi | Planktonic foraminifera from the Miocene Globigerina Marl of Hurgada Well-134, Eastern Desert, Egypt[END_REF][START_REF] Purser | The sedimentary evolution of the Red Sea rift: a comparison of the northwest (Egyptian) and northeast (Saudi Arabian) margins[END_REF], 23-25 Ma for the Central basin area (e.g. [START_REF] Plaziat | Stratigraphy of the Egyptian syn-rift deposits: correlations between axial and peripheral sequences of the north-western Red Sea and Gulf of Suez and their relations with tectonics and eustacy[END_REF]) and ca. 23.5 Ma for the Darag basin and the Cairo-Suez areas [START_REF] Kappelman | New age determinations for the Eocene-Oligocene boundary sediments in the Fayum Depression, northern Egypt[END_REF][START_REF] Lotfy | Palaeomagnetism of Early Miocene basaltic eruptions in the areas east and west of Cairo[END_REF] suggesting a rift propagation toward the north that is consistent with recent observation from the Nile delta [START_REF] Sarhan | Late Miocene normal faulting beneath the northern Nile. Delta: NNW propagation of the Gulf of Suez Rift[END_REF].

Two preserved depocenters 50-60 km wide are localized over the future main Southern and Central domains of the Suez rift (Figure 5a). To the North, there is no data from the Darag basin depocenter to illustrate Oligocene deposits but only few witnesses in the northernmost part of the Suez rift (Figure 5a). The central part is also characterized by volcanism along the rift shoulders and rift axis (Figure 5a). Basaltic dikes, sills and flows have sub-alkaline to alkaline affinities and have been interpreted to be diagnostic of intraplate, tensional environment [START_REF] Moussa | Geologic studies and genetic correlation of basaltic rocks in west central Sinai[END_REF].

Subsidence was very low during the Late Oligocene [START_REF] Steckler | Uplift and extension at the Gulf of Suez: indications of induced mantle convection[END_REF][START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF] and reliefs mainly corresponded to inherited topography from the Syrian Arc such as the Wadi Araba structure [START_REF] Garfunkel | Relation between continental rifting and uplifting: evidence from the Suez rift and northern Red Sea[END_REF]Evans 1990;[START_REF] Khaled | Rift architecture and growth sedimentation across a main accommodation zone, Northern Gulf of Suez -Egypt[END_REF]; Figure 1). Basement was already exposed to the South (present day Red Sea) by late Oligocene times [START_REF] Thiriet | Evolution tectonique et sédimentaire de la marge occidentale de la Mer Rouge au Néogène de Port Safaga (Egypte)[END_REF]. The onset of rift-related uplift in Sinai has been proposed around 26.6 +/-3 Myr based on Fission Track Analysis [START_REF] Kohn | History of uplift of the crystalline basement of Sinai and its relation to opening of the Red Sea as revealed by fission track dating of apatites[END_REF].

Rift widening (Miocene, ~Aquitanian, ca. 3Myr duration)

The presence of growth-strata in the Nukhul Fm indicates that extensional faults were active during the Aquitanian (e.g. [START_REF] Colletta | Longitudinal evolution of the Suez rift structure (Egypt)[END_REF][START_REF] Jackson | Growth and linkage of the East Tanka fault zone, Suez rift: structural style and syn-rift stratigraphic response[END_REF]. The rift was subdivided into numerous depocenters (Figure 5b) controlled by active faults recording a progressive fault linkage and interaction (e.g. [START_REF] Leeder | Sedimentary models for extensional tilt-block/halfgraben basins[END_REF][START_REF] Gawthorpe | Linked sequence stratigraphic and structural evolution of propagating normal faults[END_REF][START_REF] Khalil | Extensional fault-related folding, northwestern Red Sea, Egypt[END_REF][START_REF] Jackson | Growth and linkage of the East Tanka fault zone, Suez rift: structural style and syn-rift stratigraphic response[END_REF]. Meanwhile, some former faults were abandoned. This first major phase of extension was characterized by a low tectonic subsidence (0-100m/Myr, [START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF]. The Nubia Sandstones and the crystalline basement were the main feeding sources for sediment delivery into the Southern basin. Scarce boulder conglomerates and breccias suggest high local relief in the Central basin as well as in the Southern basin (e.g. [START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF][START_REF] Patton | Tectonic evolution and structural setting of the Suez Rift[END_REF]Winn et al. 2001), that is consistent with the initiation of basement uplift along the western margin of the Gulf of Suez between 21 and 23 Ma based on fission track analysis [START_REF] Omar | Fission-track analysis of basement apatites at the western margin of the Gulf of Suez rift, Egypt: evidence for synchronicity of uplift and subsidence[END_REF]).

These very coarse-grained deposits could also be locally related to fault block rotation and exposure of the footwall crests. Sedimentological and structural evidences suggest an overall subdued topography with perhaps only a few hundreds of meters relief that is consistent with previous works [START_REF] Garfunkel | The tectonics of the Suez rift[END_REF][START_REF] Sellwood | Facies evolution in the Gulf of Suez area: sedimentation history as an indicator of rift initiation and development[END_REF].

Rift climax (Miocene, ~Burdigalian, ca. 5Myr duration)

Rotation and uplifting of fault blocks as well as renewing subsidence were recorded all over the basin during the latest Aquitanian-earliest Burdigalian period of time (Post Nukhul Event;[START_REF] Garfunkel | The tectonics of the Suez rift[END_REF]Beleity 1984;[START_REF] Chenet | Some observations on the rift tectonics in the eastern part of the Suez rift[END_REF]. The rift was subdivided into some major basins controlled by active faults highlighting the three main domains of the Suez rift (Figure 5c). Fault linkage still occurred. Tectonic subsidence rates increased (up to 250 m/Myr) and the total subsidence rates were as high as 400 m/Myr in the deeper, more rapidly subsiding grabens [START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF]. Subsidence rates in the Gulf of Suez reached their maximum during the Burdigalian and occurred across the entire rift basin [START_REF] Steckler | Uplift and extension at the Gulf of Suez: indications of induced mantle convection[END_REF][START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Moretti | The evolution of the Suez rift: a combination of stretching and secondary convection[END_REF][START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF]. Concomitantly, the shoulders of the rift, including the Sinai Massif and Red Sea Hills, underwent rapid uplift [START_REF] Garfunkel | The tectonics of the Suez rift[END_REF][START_REF] Garfunkel | Relation between continental rifting and uplifting: evidence from the Suez rift and northern Red Sea[END_REF]).

The mid-Clysmic event is interpreted as a major tectonic reactivation in the rift which involved the segmenting and rotation of major pre-existing tilted blocks into smaller units [START_REF] Garfunkel | The tectonics of the Suez rift[END_REF]. To the north of the Suez rift, tectonic subsidence ceased completely [START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF]. It corresponds to a major pulse in siliciclastics (at least two times the mean sediment supply during the whole rifting, Figure 6). Moreover, the sediment supply pulse is probably underestimated in our study as we used a duration of 0.9 Myr for R1 and R2 following a simple linear interpolation for the duration of each phases during the Rudeis Fm deposition, while a 0.5 Myr duration would be more likely. It is also concomitant with a major eustatic sea level fall (Gradstein et al. 2012).

Late syn-rift to rift narrowing (Miocene, ~Langhian-Serravalian, ca. 4Myr duration)

During the Langhian, the rift was subdivided into several main depocenters controlled by active faults that were superimposed onto the previous Rudeis depocenters (Figure 5d). New additional depocenters localized along the rift margin suggest a widely distributed and overall basinal subsidence (Figure 5d).

The Rudeis to Kareem transition (~ early Langhian) was characterized by a major decrease of the extension rate, especially in the vicinity of Hurghada from 0.48 to 0.18 cm/yr [START_REF] Steckler | Subsidence in the Gulf of Suez: implications for rifting and plate kinematics[END_REF]). The former reliefs induced during the rift climax were quickly destroyed as evidenced by the drastic drop in sediment supply (Figure 6). Stratigraphic architecture along the eastern margin suggests that some of the main border faults became inactive and fault activity migration toward the basin axis (e.g. Baba area; Figure 3, Figure 4).

The Kareem to Belayim transition (~ late Langhian) was then characterized by another major decrease of the extension rate from 0.18 to 0.05 cm/yr [START_REF] Steckler | Subsidence in the Gulf of Suez: implications for rifting and plate kinematics[END_REF]). Subsidence analysis also indicates a sudden drop in subsidence rates at the end of the Kareem Fm deposition [START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF]. During Serravalian times, the rift was subdivided into several main depocenters mainly localized along the present day basin axis (Figure 5e). While tectonic subsidence rate was almost negligible during Serravalian times, accommodation space creation was mainly controlled by sediment loading [START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF] along the basin axis indicating a major rift narrowing (Figure 5e, Figure 6).

Tectonic quiescence to latest syn-rift (Miocene, ~Tortonian-Messinian, ca. 7Myr duration)

The basin was still subdivided into several sub-basins bounded by major faults already well developed during the previous rift narrowing stage (Figure 5f,5g). Tectonic subsidence was negligible and accommodation space creation was mainly controlled by sediment loading [START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF]. To the north of the Suez rift, tectonic uplift could have occurred [START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF]. Sedimentary patterns and fauna indicate that the rift was definitively disconnected from the Mediterranean Sea.

DISCUSSION

Rift evolution and sediment supply

The large scale evolution of the Suez rift is consistent with other published models for rift evolution with a (1) Rift Initiation, (2) Rift widening, (3) Rift climax, (4) Late syn-rift to rift narrowing and (5) Tectonic quiescence to latest syn-rift [START_REF] Leeder | Sedimentary models for extensional tilt-block/halfgraben basins[END_REF][START_REF] Prosser | Rift-related linked depositional systems and their seismic expression[END_REF][START_REF] Lambiase | Structural controls on sedimentation in continental rifts[END_REF][START_REF] Gawthorpe | Tectono-sedimentary evolution of active extensional basins[END_REF]. Our study provides some additional constraints in terms of timing and erosion/sedimentation dynamics within the rift evolution (Figure 6). The mass balance analysis indicates that the rift shoulder dynamic includes a growth phase lasting 6-7 Myr recorded by an rapid and progressive increase in sediment supply (Figure 6). Relief then reached its topographic maximum as suggested by the maximum sediment supply (Latest Rudeis Fm, R5). Finally, the rapid and abrupt decrease in sediment supply (ca. 1Myr) during the transition from the Rudeis Fm to Kareem Fm, was followed by a progressive decrease (ca. <3.5Myr duration, Kareem to Belayim Fms) to reach a very low value during the South Gharib Fm deposition. This final evolution can be interpreted as a "relief destruction" phase. This sediment supply dynamic at rift scale is consistent with analog and numerical modeling (growth phase, optimum and destruction phase), clearly indicating that this sediment supply dynamics was tectonically driven (e.g. [START_REF] Lague | Laboratory experiments simulating the geomorphic response to tectonic uplift[END_REF][START_REF] Bonnet | Landscape response to climate change: insights from experimental modeling and implications for tectonic vs. climatic uplift of topography[END_REF][START_REF] Rohais | Sedimentary record of tectonic and climatic erosional perturbations in an experimental coupled catchment-fan system[END_REF]. This result has a major impact onto the understanding of flank retreat dynamic during post-rift evolution. Indeed, most of the concept and modeling approaches addressing flank retreat issue are based on a starting boundary condition using former rift topography (e.g. [START_REF] Lyon | Mechanisms of extensional basin formation and vertical motions at rift flanks: constraints from tectonic modeling and fission-track thermochronology[END_REF][START_REF] Brown | Denudational history along a transect across the Drakensberg Escarpment of southern Africa derived from apatite fission track thermochronology[END_REF][START_REF] Japsen | Elevated, passive continental margins: Not rift shoulders, but expressions of episodic, post-rift burial and exhumation: Global and Planetary Change[END_REF]). In our study, the sediment supply dynamic indicate that the latest syn-rift phase was characterized by low relief with very localized inputs of siliciclastics (Figure 4, Figure 6). This point could be considered as a major challenge in some future works. Typically, in the Suez rift, the present day topography is potentially related to the post-rift dynamics.

Suez rift and geodynamic setting

At 14 Ma (Langhian), the Aqaba transform boundary cut through Sinai and the Levant continental margin (Figure 1), linking the northern Red Sea with the Bitlis-Zagros convergence zone (e.g. [START_REF] Bosworth | The Red Sea and Gulf of Aden Basins[END_REF][START_REF] Gvirtzman | Inland jump of the Arabian northwest plate boundary from the Levant continental margin to the Dead Sea Transform[END_REF]. Extension in the Suez was reduced and then stopped (e.g. [START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Steckler | Subsidence in the Gulf of Suez: implications for rifting and plate kinematics[END_REF] suggesting that the mechanism responsible for the Suez rift opening was no more active.

Meanwhile, the opening of the Red Sea continued until became an ocean during the Pliocene.

Extension in the Suez rift has been previously reduced during the Langhian times in response to the collision of Arabia and Eurasia [START_REF] Dercourt | Geological evolution of the Tethys belt from the Atlantic to the Pamirs since the Lias[END_REF][START_REF] Pichon | The rotation of Arabia and the Levant fault system[END_REF].

The Aqaba transform boundary (Figure 1) could thus be interpreted as an accommodation fault between the continuous extensional processes in the southern Red Sea and an abandoned extensional segment in the north corresponding to the Suez rift. It suggests that the deep source controlling the extension in the Suez rift is not below the rift, but below the Red Sea. This is very consistent with a south to north propagation of the Suez rift as documented in our reconstruction (Figure 4).

Evaporite in rift basin

Evaporite deposition is generally controlled by the combined effect of (1) the hydrologic balance, or aridity index and (2) the isolation of the basin characterized by the interaction between sill and sea level (e.g. [START_REF] Warren | Evaporites through time: Tectonic, climatic and eustatic controls in marine and nonmarine deposits[END_REF]). Regarding the aridity, a global cooling and drying at about 15.6 Ma (i.e. Langhian) occurred in northeastern Africa (Kennett, 1995). In the late Tortonian -Early Messinian (ca. 8 Ma) relatively more humid conditions occurred in an overall arid setting [START_REF] Griffin | The late Miocene climate of north-eastern Africa: unravelling the signals in the sedimentary succession[END_REF], that is consistent with our reconstructions for the Zeit Fm (Messinian). During the Plio/Pleistocene northeastern Africa was still subjected to alternating dry and wet periods [START_REF] Griffin | The late Miocene climate of north-eastern Africa: unravelling the signals in the sedimentary succession[END_REF]2002). Aridification was thus a criterion satisfied for evaporite deposition in the Suez rift starting from the Langhian times.

The main sills were in the north of the Darag basin and across the Zaafarana and Morgan accommodation zones (Figure 1). The first evidence for the isolation of the Suez rift occurred during the Langhian (Kareem Fm) with a progressive paleo-bathymetry decrease along the basin axis (Darag, Central and Southern basins) and the occurrence of a large platform across the Central basin (Figure 4h-j). This "Plaform Evaporite" sensu [START_REF] Warren | Evaporites through time: Tectonic, climatic and eustatic controls in marine and nonmarine deposits[END_REF] has progressively been widened to finally reach a "Basinwide Evaporite" sensu [START_REF] Warren | Evaporites through time: Tectonic, climatic and eustatic controls in marine and nonmarine deposits[END_REF] configuration during the Serravalian times (Belayim Fm). Finally, the main sill controlling the disconnection of the Mediterranean Sea from the Red Sea were located in the north of the Darag basin during the Tortonian to Messinian times (Figure 4). It indicates that the first sills to interact with the sea level changes were related to rift structures: the Zaafarana and Morgan accommodation zones. Finally, a sill on the northern edge of the Suez rift was the dominant structure controlling the connection between Mediterranean Sea and the Red (Figure 4).

The pre-salt to salt transition in the Suez rift can thus be interpreted as a sedimentary record of the combined effect of a climate change (including aridity) and the rift dynamic that lasted for ca. 4 Myr. Finally, the occurrence of long lasted and widespread evaporite series where controlled by both two major external controlling factors: climate and geodynamic (rift abandonment).

Rift dynamic and sequence stratigraphy

A typical rift sequence can be derived from this basin-scale study. The Nukhul Fm with dominantly shallow water deposits can be interpreted as the records of the filled phase, the Rudeis Fm with its well-developed turbiditic packages as the underfilled phase, the Kareem and Belayim Fms with their prograding patterns and progressive evolution toward shallow water deposits as a filled phase and finally the South Gharib and Zeit Fms with the alluvial to sabkha deposits as overfilled phase. During filled and overfilled phases, a longitudinal N-S depositional gradient prevailed (Figure 4). This tectonically-controlled stratigraphic framework can be correlated to a second-order cycle, i.e. 18-20 Myr duration cycle. This cycle can be interpreted in a transgressive, highstand and lowstand system tracts sensu [START_REF] Catuneanu | Towards the Standardization of Sequence Stratigraphy[END_REF]. At higher resolution, the highstand system tract (Rudeis, Kareem and Belayim Fms) can be subdivided into one basal highstand (Lower Rudeis Fm) overlain by a falling stage system tract (Upper Rudeis, Kareem and Belayim Fms, Figure 2). This falling stage system tract can be subdivided into two third order sequences including two major aggrading-prograding packages that can be interpreted as lowstand system tract (Rahmi-Markha Mb. and Baba-Sidri-Feiran Mbs.; Figure 2). Duration and timing of these major third order sequences are correlated with the main tectonic stage identified for the rift evolution.

The typical rift sequence thus includes: a (1) Rift Initiation, rapid flooding and major transgressive surface, (2) Rift widening, transgressive system tract, (3) Rift climax, highstand system tract and condensed sections, (4) Late syn-rift to rift narrowing, falling stage system tract and (5) Tectonic quiescence to latest syn-rift, lowstand system tract. At higher resolution, i.e. fourth and higher order sequences, the whole cycle is not always easily identified. Sequence boundaries are often superimposed by sharp flooding surface rapidly overlain by a prograding and shallowing upward packages interpreted as highstand system tract (Figure 2). These fourth and higher order sequences could thus be related to stage of activity during the fault growth. Myr duration) characterized by several major anoxic events, maximum fault throw and subsidence rate, increasing and maximum sediment supply from the rift evolution, (4) a late syn-rift to rift narrowing (ca. 4 Myr duration) characterized by a progressive smoothing of the paleogeography with low to no more active tectonic uplift/erosion along the rift shoulders combined with a reducing paleo-bathymetry along the basin axis, (5) and finally a tectonic quiescence phase (ca. 7 Myr duration) characterized by a thick salt series.

Second, the sediment supply dynamics during rifting is characterized by (1) progressive increase up to its (2) maximum, (3) rapid and abrupt decrease (less than 1Myr) and finally (4) very progressive decrease that can be interpreted as a (1) relief growth, (2) optimum and [START_REF][END_REF]4) destruction phases related to uplift dynamic.

Third, the pre-salt to salt transition in the Suez rift is interpreted as the sedimentary record of the combined effect of a climate and rift dynamic changes. The Central basin, Zaafarana and Morgan accommodation zones were the first main divides between the Mediterranean Sea and the Red Sea.

Fourth, several order of sequences can be recognized in the syn-rift fill with fourth to higher order sequences related to fault activity, third order sequences related to (sub-)basin dynamics (Darag, Central and Southern basins) and second order sequences related to the whole rift basin dynamic (Suez rift).

The proposed geological scenario with quantified sediment supply, accumulation rate, lithologic distribution and subsidence dynamics could be used to test modeling approaches of the relationship between deep and surface processes in future works.

FIGURE CAPTION

Figure 1 A. Structural map of the Suez rift (modified from [START_REF] Colletta | Longitudinal evolution of the Suez rift structure (Egypt)[END_REF][START_REF] Patton | Tectonic evolution and structural setting of the Suez Rift[END_REF][START_REF] Bosworth | Structural and stratigraphic evolution of the Gulf of Suez rift, Egypt: a synthesis[END_REF][START_REF] Peijs | The Gulf of Suez rift basin[END_REF]). Hatched areas indicate major accommodation zones. Red lines correspond to the two cross sections presented in Figure 3. B. Geodynamic setting of the Gulf of Suez (modified from [START_REF] Bosworth | The Red Sea and Gulf of Aden Basins[END_REF]. Major elements of the Aqaba-Levant intra-continental transform boundary, the Bitlis-Zagros convergence zone and the Red Sea -Gulf of Aden are highlighted. The red rectangle shows the Gulf of Suez that corresponds to the NW termination of the Red Sea. C. Simplified stratigraphic column of the Suez rift (modified from EGPC 1964; [START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF][START_REF] Patton | Tectonic evolution and structural setting of the Suez Rift[END_REF][START_REF] Bosworth | Structural and stratigraphic evolution of the Gulf of Suez rift, Egypt: a synthesis[END_REF][START_REF] El-Naby | Sequence-stratigraphic interpretation of structurally controlled deposition: Middle Miocene Kareem Formation, southwestern Gulf of Suez, Egypt[END_REF].

Figure 2 Synthetic stratigraphic setting for the syn-rift succession of the Suez rift. Lithologies are derived from different wells to illustrate the typical sedimentary character of each formation. Silty rich for restricted deposits in green versus mud rich for offshore deposits in light blue. The association zones, main environment of deposition (EOD) and dominant paleoenvironmental conditions are modified from Hughes et al. (1992). Sequences are modified from [START_REF] Wescott | Modern applications of biostratigraphy in exploration and production[END_REF] and [START_REF] Krebs | Graphic correlation and sequence stratigraphy of Neogene rocks in the Gulf of Suez. In Fauna, flora and sequence stratigraphy[END_REF]. Colour code for system tracts: blue= transgressive, red= highstand and falling stage, orange= lowstand. Figure 4 Maps with dominant lithologies for the Nukhul Fm (a-c, ca. Aquitanian), Rudeis Fm (d-g, ca. Burdigalian), Kareem Fm (h-k, ca. Langhian), Belayim Fm (l-o, ca. Serravallian), South Gharib Fm (p-q, ca. Tortonian) and Zeit Fm (r-s, ca. Messinian). Time intervals are approximated using association zones from Hughes et al. (1992). Shales are subdivided into silty rich for restricted deposits in green versus mud rich for offshore deposits in light blue. Paleobathymetries are estimated using the results of Hughes et al. (1992). Only the deepest parts are highlighted to keep the maps readable. See Figure 1 for further information about the keys.

Figure 5 Main depocenters and distribution of the syn-rift deposits for the main stratigraphic units of the Suez rift. a. Oligocene -Chattian. b. Nukhul Fm, cut-off to highlight depocenters at 300 m. c. Rudeis Fm, cut-off to highlight depocenters at 1000 m. d. Kareem Fm, cut-off to highlight depocenters at 400 m. e. Belayim Fm, cut-off to highlight depocenters at 200 m. f. South Gharib Fm, cut-off to highlight depocenters at 900 m. g. Zeit Fm, cut-off to highlight depocenters at 600 m. See Figure 1 for further information about the keys.

Figure 6

Synthesis for the pre-salt and salt deposits of the Suez rift of evaporite and carbonate accumulation rate (km 3 /Myr), mean sediment supply (km 3 /Myr) and cumulative tectonic subsidence curves (modified from the wells analysed by [START_REF] Moretti | Spatial and temporal evolution of the Suez Rift subsidence[END_REF][START_REF] Richardson | The Gulf of Suez-northern Red Sea Neogene rift: a quantitative basin analysis[END_REF]. The grey area includes all the wells analysed for estimating the cumulative tectonic subsidence. The chronostratigraphy, microfossil biozones and sea-level curve are derived from [START_REF] Ghorab | Oligocene and Miocene rock stratigraphy of the Gulf of Suez region, unpublished report consultatus stratigraphic committee of the EGPC[END_REF]. Relative proportions of lithology for each map have been combined with thickness map to estimate the accumulation rate and sediment supply. See text for further information.

  Fm deposition the three main basins were characterized by different depositional setting suggesting a N-S paleogeographic gradient, the Rudeis Fm progressively recorded deep open marine condition all along its axis from the Darag to the Southern basin (Figure 4d-g). The Southern basin and Morgan accommodation zone were preferentially fed by siliciclastics in response to the Precambrian basement denudation, while the Darag basin was mainly characterized by carbonate dominated deposits (Figure 4d-g). Siliciclastics sources were distributed all along the rift bounding faults. Very coarse-grained conglomerate sources were localized on the steep relief located on the eastern side of the rift (Figure 4d-g).

  have been carried out to propose a basin-scale model evolution for the pre-salt to salt syn-rift fill of the Suez rift. Four main results can be highlighted from our study: First, the key periods of time during a rift evolution have been recognized and their durations have been estimated with (1) a rift initiation or onset of the rifting stage (ca. 1-4 Myr duration) with active volcanism and isolated depocenters, (2) a rift widening stage (ca. 3 Myr duration) with a progressive marine flooding and fault propagation, (3) a rift climax (ca. 5

Figure 3 (

 3 Figure 3 (A) and (B) N-S cross sections flattened on the top Zeit marker (locally base Pliocene when top Zeit Fm is not preserved) showing the distribution of the main depositional units (A) and the dominant lithologies (B) within each sub-basins and across the two accommodation zones. (C) and (D) E-W cross section flattened on the top Zeit marker (locally base Pliocene when top Zeit Fm is not preserved) showing the distribution of the main depositional units (C) and the dominant lithologies (D) within the Central Basin. Sections cross-cut at well 13.

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TABLE CAPTION Table 1

 CAPTION1 Results of the mass balance characterization of the pre-salt to salt syn-rift deposits of the Suez rift. The preferred scenario is highlighted in grey. See text for further explanation.

			Stratigraphy	Groups and Formations Litho.	Rifting Phases
			Pliocene -Pleistocene		Post-Zeit	POST	-RIFT
		CENOZOIC	Miocene	Early Middle Late	Gharandal Group Ras Malaab Gr.	Zeit South Gharib Nukhul Rudeis Kareem Belayim	SYN-RIFT
			Oligocene		Abu Zenima
			Paleocene Early Eocene Late	El Egma Group	Darat Thebes Esna Shale Sudr Chalk
		MESOZOIC	Late Cretaceous	Ceno-manian Turonian Senonian	Nezzazat Group	Brown Lm -Duwi Matulla Wata Abu Qada Raha	PRE-RIFT
			Jurassic -Lower Cretaceous		Nubia "A"
	Red Sea	PALEOZOIC	Carboniferous Cambrian to Devonian		Nubia "B" Nubia "C and D"
		PRE-CAMBRIAN		Basement

Acknowledgements

This project could not have been accomplished without the very large database acquired by IFPEN during the last 30 years in the frame of collaborative partnerships. The authors would like to thank the two anonymous reviewers for their valuable suggestions and reviews of the initial manuscript.