A model study of the seasonality of sea surface temperature and circulation in the Atlantic North-eastern Tropical Upwelling System

Probably not a substantial claim: may not pass S3 (load-bearing).

A wind-derived proxy indicates that upwelling persists in summer from 15 to 20°N, albeit weaker.

“One may wonder how much it contributes to the SST warming and what are the upwelling real cycle and effects, since a wind-derived proxy indicates rather that the latter persists in summer from 15 to 20 • N, albeit weaker [e.g., 3].”

• cites [3] Lathuilière, 2008, Seasonal and intraseasonal surface chlorophyll-a variability along the northwest African coast, J Geophys Res sourceSupported

Probably not a substantial claim: may not pass S3 (load-bearing).

The North Equatorial Counter-Current has a large seasonal cycle.

“South of the region, the circulation is dominated by the North Equatorial Counter-Current (NECC), which has a large seasonal cycle [13,14].”

• cites [13] Mittelstaedt, 1991, The ocean boundary along the northwest African coast: circulation and oceanographic properties at the sea surface, Prog Oceanogr sourceNot checked — no full text of the source
• cites [14] Stramma, 2005, Water masses and currents in the upper tropical northeast Atlantic off northwest Africa, J Geophys Res. sourceSupported

Probably not a substantial claim: may not pass S3 (load-bearing). May combine two claims.

Foltz et al. find that air-sea fluxes drive the climatological SST seasonal cycle in the western part of the domain and suggest from the heat budget residual that vertical mixing damps it.

“They find also that air-sea fluxes drive the cycle, and suggest, from the heat budget residual, that vertical mixing damps it.”

• cites [22] Foltz, 2013, Seasonal cycle of the mixed layer heat budget in the Northeastern Tropical Atlantic Ocean, J Clim. sourceSupported

Probably not a substantial claim: may not pass S3 (load-bearing).

Yu et al. evidenced a very high correlation at large scale in the region north of 10°N between the SST time derivative and the net air-sea flux.

“Yu et al. [21] on the other hand evidenced the very high correlation at large scale in the region north of 10 • N between the SST time derivative and the net air-sea flux.”

• cites [21] Yu, 2006, Role of net surface heat flux in seasonal variations of sea surface temperature in the tropical Atlantic Ocean, Clim J. sourceSupported

May combine two claims.

The diffusive warming and inversions distribution results from a combination of the large-scale barrier layer distribution associated with the ITCZ and NECC, and from a narrow coastal band reaching further north up to the Cape Verde Peninsula, likely due to advection of equatorial fresh waters by the SLJ as well as local seasonal rainfall.

“Looking at the diffusive warming and inversions distribution, it appears that it results from a combination of the large scale barrier layer distribution associated with the ITCZ and NECC [41], and from a narrow coastal band reaching further north up to the Cape Verde Peninsula, likely due to advection of equatorial fresh waters by the SLJ as well as local seasonal rainfall.”

• cites [41] Mignot, 2012, On the formation of barrier layers and associated vertical temperature inversions: a focus on the northwestern tropical, J Atlantic Geophys Res sourcePartly supported

  Split into 2 atoms — 0 confirmed, 2 partially supported, 0 disputed, 0 misattributed, 0 unverifiable. Expand the claim to see per-atom verdicts.

  Experimental — accuracy not yet measured

Probably not a substantial claim: may not pass S3 (load-bearing). May combine two claims.

The tropical upwelling system forces a cyclonic gyre circulation, the Guinea Gyre, of which the Guinea Dome and coastal West-African upwellings form the most eastern features.

“Considered from a basin-scale perspective, this system forces a cyclonic gyre circulation, the Guinea Gyre [e.g., 6], of which the Guinea Dome and the coastal West-African upwellings form the most eastern features [4,7].”

• cites [6] Jiang, 2008, Role of gyration in the oceanic general circulation: Atlantic Ocean, J Geophys Res sourceSupported
• cites [4] Siedler, 1992, Seasonal changes in the tropical Atlantic circulation: observation and simulation of the Guinea Dome, J Geophys Res. sourceNot checked — no full text of the source
• cites [7] Yamagata, 1995, Simulation of the tropical thermal domes in the Atlantic: a seasonal cycle, J Phys Oceanogr sourceNot checked — no full text of the source

Probably not a substantial claim: may not pass S3 (load-bearing).

In the tropical Atlantic, SST exerts a significant influence on the climate of surrounding regions.

“In the tropical Atlantic, as well as for the other tropical basins, SST exerts a significant influence on the climate of surrounding regions (e.g., [1,2]).”

• cites [1] Carton, 1994, Warm events in the Tropical Atlantic, J Phys Oceanogr sourceNot checked — no full text of the source
• cites [2] Chang, 2006, Climate fluctuations of tropical coupled systems: the role of ocean dynamics, J Clim sourceSupported

May combine two claims.

Around the Cape Verde Archipelago and south of about 15°N, horizontal advection explains in large part the net ocean contribution, with intensities generally larger than those of vertical processes.

“To the contrary, around the CVA and south of about 15 • N, the advection pattern explains in large part the net ocean contribution, with intensities generally larger than those of vertical processes.”

May combine two claims.

The large-scale patterns of the model SST change during the cooling period are comparable to observations, with only a slight underestimation of cooling of about 0.2°C per month near the coast from 14° to 20°N.

“The large-scale patterns of the model are comparable to those of the observations, with only a slight underestimation of the cooling (∼0.2 • C.month -1 ) near the coast from 14 • to 20 • N.”

May combine two claims.

South of about 12°N, the warming longitudinal band is due to geostrophic Mauritania Current and Ekman drift poleward transports, while the cooling pattern to the south-east is explained by the equatorward component of the North Equatorial Counter-Current and the Ekman currents.

“Finally, to the south of ∼12 • N, the warming longitudinal band is due to geostrophic MC and Ekman drift poleward transports, whereas the cooling pattern to the south-east is explained by the equatorward component of the NECC and the Ekman currents.”

May combine two claims.

The model mixed layer depth is 10-30 m too deep during the cooling period and about 5 m too shallow during the warming period.

“The model MLD is 10-30 m too deep during CP and about 5 m too shallow during WP.”

May combine two claims.

Vertical mixing in summer-autumn tends to cool the surface north of the ITCZ and warm the surface south of the ITCZ.

“Vertical mixing in summer-autumn tends to cool (warm) the surface north (south) of the ITCZ”

May combine two claims. The quote only partly states this claim.

West of 18-19°W, vertical temperature gradients at the mixed layer base reach maximum intensities about five times larger than nearshore, explaining the vast and moderate diffusion pattern.

“The vertical temperature gradients at the mixed layer ML base reach maximum intensities, about five times larger than nearshore (Figure 7D), explaining the vast and moderate diffusion pattern.”

May combine two claims.

During the cooling period, the ocean contribution displays the larger negative signals, whereas during the warming period, the net air-sea flux contribution is larger.

“As we will see, during CP, the ocean contribution displays the larger negative signals, whereas during WP, it is the net air-sea flux contribution.”

May combine two claims.

The large-scale structure of the temperature change during the warming period is very similar to the cooling period with a sign reversal and a somewhat more rapid evolution, with maxima of about 1°C per month.

“The large-scale structure of the temperature change during WP is very similar with a sign reversal and a somewhat more rapid evolution (maxima ∼1 • C.month -1 , Figure 3C).”

May combine two claims.

During the warming period the North Equatorial Counter-Current seems slightly reinforced by Ekman drift in the model and observations and turns into the Guinea Current to the south and into a northern circulation branch that is particularly intense at the coast.

“During WP the NECC seems slightly reinforced by Ekman drift in the model and observations and turns into the Guinea Current to the South and into a northern circulation branch, particularly intense at the coast.”

May combine two claims.

South of 12°N, vertical processes sustain a vast warming effect, albeit weak except along-shore, indicating the influence of temperature inversions.

“South of 12 • N, a remarkably vast warming effect, albeit weak except along-shore, is sustained by vertical processes, which indicate the influence of temperature inversions”

May combine two claims.

During the cooling period, the air-sea heat flux contribution has a coastal maximum, a rapid decrease until near 18°W where the sign changes, and a moderate decrease westward.

“The general structure is hence a coastal maximum, a rapid decrease until near 18 • W where the sign changes, and a moderate decrease westward.”

May combine two claims.

The strongest upwelling velocities are located nearshore north of about 10°N, reaching values of the order of 100 m per month during the cooling period and 50 m per month during the warming period.

“The strongest upwelling velocities are located nearshore north of ∼10 • N, where they reach values of the order of 100 (resp.50) m.month -1 during CP (resp.WP).”

May combine two claims.

During the cooling period, the maximum along-shore vertical cooling intensities are due to stronger vertical diffusivity there, not to vertical temperature gradients, which are weak compared to offshore.

“It appears that the maximum intensities along-shore is due to stronger vertical diffusivity there (Figure 7C), not to vertical temperature gradients which are weak compared to offshore (Figure 7D).”

May combine two claims.

South of 12°N, both the Sierra Leone Jet and the southward Ekman currents flow in large part along homogeneous warm SST and are thus less important for SST change.

“South of 12 • N, both the SLJ and the southward Ekman currents are flowing in large part along homogeneous warm SST, and become thus less important for the SST change.”

May combine two claims.

Along south Mauritania and northern Senegal from 20 to 15°N, the coastal jet is not systematically causing cooling; cooling instead results from the ageostrophic flow.

“Hence along south Mauritania and northern Senegal from 20 to 15 • N, the CJ is not systematically causing cooling, which instead results from the ageotrophic flow.”

The quote only partly states this claim.

Offshore upwelling velocities display values one order of magnitude lower than nearshore.

“Offshore, upwelling velocities display one order of magnitude lower values.”

May combine two claims.

The annual mean ocean warming effect south of 12°N is dominated by advection of warm waters poleward by the North Equatorial Counter-Current, except alongshore where currents are weak and SST is warmed by temperature inversions.

“The ocean warming effect is however dominated by advection of warm waters poleward by the NECC (Figure 6C), except alongshore where currents are weak and SST is warmed up also by temperature inversions (Figure 6B).”

May combine two claims.

The Canary Current exhibits important seasonal variability with strengthening during the warming period in association with stronger winds in the north.

“The CC exhibits an important seasonal variability with a strengthening during WP in association with stronger winds in the north (Figures 5B,D).”

May combine two claims.

North of about 12°N, vertical processes cause general cooling through vertical exchanges with colder subsurface waters and prevail over horizontal processes by a factor of about two in large parts of the domain.

“North of ∼12 • N, vertical processes cause an expected general cooling through vertical exchanges with colder subsurface waters.It is worth noting that they prevail over the horizontal ones by a factor of about two in large parts of the domain”

May combine two claims.

Compared to the annual mean, during the cooling period vertical processes cause stronger cooling in the 12-18°N coastal upwelling band and weaker cooling in the 18-24°N band, associated with the latitudinal structure of seasonal Ekman pumping changes.

“Compared to the annual mean, the vertical processes cause a stronger (weaker) cooling in the 12-18 • N (18-24 • N) coastal upwelling band (Figure 7B), evidently associated with the latitudinal structure of the seasonal Ekman pumping changes.”

May combine two claims.

The mixed layer depth is shallower at the coast by a factor of 1.5-2 relative to further west, amplifying the effect of the diffusive flux at the coast.

“Indeed, MLD, which enters the diffusive flux term in the denominator, is shallower at the coast by a factor of 1.5-2 relative to further west.”

May combine two claims.

Oceanic processes significantly oppose the open ocean SST cycle, except for winter north of about 18°N.

“The oceanic processes significantly oppose it, but for winter north of ∼18 • N.”

May combine two claims.

Zonally, annual mean ocean contributions are maximum at the coast with values up to -5°C per month and decrease abruptly westward by an approximate factor of five over a few degrees of longitude.

“Zonally, contributions are maximum at the coast with values of up to -5 • C.month -1 , and decrease abruptly westward by an approximate factor of five over a few degrees of longitude (Figure 6A).”

May combine two claims.

From 15 to about 12.5°N, the balance is comparable to north of Cape Timiris, and there is a net cooling effect explained essentially by the coastal jet.

“From 15 to about 12.5 • N, the balance is comparable to north of Cape Timiris.There is a net cooling effect explained essentially by the CJ.”

May combine two claims.

The maximum net cooling at latitudes 12-16°N is due to westward advection of coastal waters by Ekman drift to the east and to southward advection by the Guinea gyre geostrophic circulation to the west.

“In particular, the maximum net cooling visible at latitudes 12-16 • N appears to be due, to the east, to westward advection of coastal waters by Ekman drift (Figure 8B) and, to the west, to southward advection by the Guinea gyre geostrophic circulation (Figure 8C).”

May combine two claims.

To the north, wind speed decreases westward and its effect on turbulent cooling is dominated by the SST increase.

“To the north the wind speed decreases westward and effect on turbulent cooling is dominated by the SST increase.”

May combine two claims.

West of 18°W, the same opposition between ocean processes and air-sea fluxes holds within the 12-18°N latitude band only, where the maximal net SST cooling centered at (16°N, 18°W) is due mainly to Ekman drift of cold coastal waters.

“West of this longitude band, the same opposition holds within the 12-18 • N latitude band only, where the maximal net SST cooling centered at (16 • N, 18 • W) (Figure 3B) is due mainly to Ekman drift of cold coastal waters.”

May combine two claims.

North of the ITCZ region, air-sea fluxes predominate over ocean processes in net SST warming; south of it, weak SST variations are dominated by the ocean contribution.

“To conclude, it is worth noting the predominance in the net SST warming of the air-sea fluxes over the ocean processes north of the ITCZ region, whereas south of it, the weak SST variations are rather dominated by the ocean contribution.”

May combine two claims.

East of 18°W, ocean processes associated with coastal upwelling dynamics dominate the time-average cooling, whereas air-sea fluxes damp it.

“East of 18 • W, the ocean processes associated with coastal upwelling dynamics dominate the time-average cooling, whereas the air-sea fluxes damps it.”

May combine two claims.

West of ∼18°W, the westward increase of trade wind speed explains the progressive passage to a more classical winter cooling regime by air-sea fluxes, except in the CVA where local wind reduction in the lee of islands generates a net heat gain by the ocean.

“West of ∼18 • W, the westward increase of the trade winds speed explains the progressive passage to a more classical winter cooling regime by air-sea fluxes, to the exception of the CVA where local wind reduction in the lee of islands generates a net heat gain by the ocean.”

May combine two claims.

Minimum heat loss occurs over cold coastal waters north of the Senegal-Mauritania front (about 12°N), and larger loss occurs over the warm Sierra Leone Jet to the south nearshore.

“Similarly one observes minimum heat loss over cold coastal waters, north of the Senegal-Mauritania front (∼12 • N), and larger loss over the warm SLJ to the south nearshore (Figure 9C).”

May combine two claims.

Off-line reconstruction of the vertical diffusion effect indicates that it is in large part explained by the vertical temperature gradient at the ML base, rather than by the vertical diffusion coefficient Kz, except for the intensified Morocco upwelling.

“Off-line reconstruction of the vertical diffusion effect indicates that is in large part explained by the vertical temperature gradient at the ML base, rather than by the vertical diffusion coefficient K z (Figures 11C,D), except for the intensified Morocco upwelling.”

May combine two claims.

Their intensities reach up to 0.6°C.month−1, corresponding to mesoscale eddy activities accompanying coastal upwelling.

“Their intensities reach up to 0.6 • C.month -1 , corresponding to mesoscale eddy activities accompanying coastal upwelling.”

May combine two claims.

The net air-sea flux decrease arises from its turbulent component only, since solar radiation absorbed in the ML increases slightly westward.

“The net air-sea flux decrease arises from its turbulent component only, since solar radiation absorbed in the ML increases slightly westward (contours in Figure 10B).”

May combine two claims.

The net air-sea flux changes sign during CP but explains month-to-month SST variations in large parts of the region.

“The net-air-sea flux in fact changes sign during CP, but explains month-to-month SST variations in large parts of the region, as we will see in Section The Sub-domain Next to the Continent.”

May combine two claims.

The zonal change in air-sea flux effect north of 15°N is due to the net air-sea flux distribution and the MLD westward increase, both explaining the zonal change in roughly equal proportion.

“It is due to the net air-sea flux distribution (Figure 10B), and also to the MLD westward increase (Figure 3D), both of them explaining the zonal change in roughly equal proportion.”

May combine two claims.

The ocean contribution general structure during WP is comparable to the annual mean, but with larger intensities to the north and south of the domain.

“Its general structure is comparable to the annual mean, but for larger intensities to the north and south of the domain.”

May combine two claims.

The seasonal variations of the SST can be described by a CP of decreasing and then minimum SST (November-May), and a WP (June-October) of increasing SST reaching a maximum in summer.

“The seasonal variations of the SST can be described by a CP of decreasing and then minimum SST (November-May), and a WP (June-October) of increasing SST reaching a maximum in summer.”

May combine two claims.

The air-sea fluxes contribution is more intense most of the time, though, since the oceanic processes oppose it quasi systematically.

“It is more intense most of the time, though, since the oceanic processes oppose it quasi systematically (Figures 14B,C).”

May combine two claims.

Around 21°N, warming occurs just at the coast because upwelling and SST minima are found at some distance offshore, due to the wide plateau which affects structure and intensity of the upwelling.

“Around this latitude, warming occurs just at the coast because upwelling and SST minima are found at some distance offshore, as observed by Barton et al. [46], due to the wide plateau which affects structure and intensity of the upwelling.”

• cites Barton et al. [46] Barton, 1977, Temporal variation observed in the hydrographic regime near Cabo Corveiro in the northwest African upwelling region, February to April 1974, Deep Sea Res. sourceNot checked — no full text of the source

May combine two claims.

Two latitudinal sectors emerge from Figure 13A: north of 12°N the SST experiences an annual cycle, whereas to the south it is semi-annual and forced by the two passages of the ITCZ.

“Two latitudinal sectors emerge from Figure 13A.North of 12 • N the SST experiences an annual cycle, whereas to the south it is semi-annual and forced by the two passages of the ITCZ (Figure 13A).”

May combine two claims.

Overall, the seasonal increase of the net air-sea flux sets the start of the warming season, whereas ocean processes act to reduce or delay the warming.

“Nevertheless, it is overall the seasonal increase of the net air-sea flux that sets the start of the warming season, whereas ocean processes act to reduce or delay the warming.”

May combine two claims.

Both periods are respectively associated with maximum then minimum coastal upwelling south of ∼20°N (Cape Timilis), and vice-versa north of the Cape.

“Both are, respectively, associated with maximum then minimum coastal upwelling south of ∼20 • N (Cape Timilis), and vice-versa north of the Cape.”

May combine two claims.

Just south of Cape Verde Peninsula, the advection of warm waters brought by the MC dominates the Ekman drift, which leads to net warming by advection.

“To the opposite, just south of Cape Verde Peninsula, the advection of warm waters brought by the MC dominates the Ekman drift, which leads to net warming by advection (Figures 12A-C).”

May combine two claims.

South of 15°N, seasonal temperature inversion effects as well as northward advection of warm waters by the MC and SLJ warm the SST.

“There, seasonal temperature inversion effects (Figure 13D) as well as northward advection of warm waters by the MC and SLJ (Figure 13E) warm the SST to the contrary.”

May combine two claims.

In the open ocean west of 18°W, the SST temporal changes are broadly similar to those next to the continent, but share a much stronger resemblance with the net air-sea flux term.

“We now focus on the area west of 18 • W. The SST temporal changes are broadly similar to those next to the continent, but share a much stronger resemblance with the net air-sea flux term (Figures 14A,B).”

May combine two claims.

The relative high intensity of the cooling effect by ocean processes is essential to the heat budget but not for its change from a net positive to net negative trend.

“The relative high intensity of the cooling effect by ocean processes is essential to the heat budget evidently, but not for its change from a net positive to net negative trend.”

May combine two claims.

Vertical turbulent processes dominate the cooling, whereas coastal horizontal currents favor or oppose them depending on latitude.

“Vertical turbulent processes dominate the cooling (see ratio in contours, Figure 13C), whereas coastal horizontal currents favor or oppose them depending on latitude, as discussed in previous sections.”

May combine two claims.

From 8 to 10°N, temperature inversions oppose the July cooling, but set the following warming.

“From 8 to 10 • N they oppose the July cooling, but set the following warming.”

May combine two claims.

Two regions of exception: north of ∼18°N when the oceanic processes contribute weakly to the forcing of the SST decrease by the air-sea fluxes (October-February), and south of 10°N in September-October when the ocean forces mainly the second semi-annual warming.

“Two regions of exception deserve attention: north of ∼18 • N when the oceanic processes contribute weakly to the forcing of the SST decrease by the air-sea fluxes (October-February), and south of 10 • N in September-October when the ocean forces mainly the second semi-annual warming.”

May combine two claims.

On the continental shelf south of 12°N, a coastal SST maximum leads to the same type of compensation between geostrophic currents (cooling) and Ekman drift (warming), with overall a weak advective effect on SST.

“On the continental shelf south of 12 • N, a coastal SST maximum leads to the same type of compensation between geostrophic currents (cooling) and Ekman drift (warming), described above for southern Morocco, with overall a weak advective effect on SST.”

May combine two claims.

The cooling phases start early September north of the Cape Verde Peninsula, and later on further south (until December).

“We first study the cooling phases, which start early September north of the Cape Verde Peninsula, and later on further south (until December).”

May combine two claims.

Two main heat budget regimes emerge in annual mean on both sides of schematically latitude 12°N (related to the mean ITCZ location) and are quite representative of the time-varying contribution of ocean processes.

“Two main heat budget regimes emerge in annual mean on both sides of schematically latitude 12 • N (related to the mean ITCZ location) and are quite representative of the time-varying contribution of ocean processes.”

May combine two claims.

In annual mean, the ocean cools the Guinea Dome SST in its northern half but warms it in its southern part.

“This shows that, in annual mean, the ocean cools the GD SST in its northern half, but warms it in its southern part.”

May combine two claims.

The northward migration of the ITCZ causes a decrease of coastal Ekman pumping south of 18°N and an increase north of it.

“The northward migration of the ITCZ causes a decrease of the coastal Ekman pumping south of 18 • N, and an increase north of it (Figure 2).”

May combine two claims.

The seasonal shift of the ITCZ is responsible for a northward shift of the open-ocean upwelling, which in turn lifts the thermocline and tends to enhance stratification north of about 15°N.

“To explain the meridional structure of the subsurface stratification, it is first necessary to recall that the seasonal shift of the ITCZ is responsible of a northward shift of the open-ocean upwelling, which in turn lifts the thermocline (Figure 4D) and tends to enhance stratification north of about 15 • N.”

Probably not a substantial claim: may not pass S3 (load-bearing), S4 (based). May combine two claims.

Differences between ratios of time-averaged group terms and ratios of 5-day outputs are of second order and not relevant to discuss in this study.

“Differences between both computations are of second order and not relevant to discuss in this study.”

May combine two claims.

The net air-sea flux is positive almost everywhere, and the net cooling contribution to the ML heat budget visible south of the ITCZ diagonal can only be due to the fraction of the solar flux that penetrates below the ML.

“However the net air-sea flux is positive almost everywhere, and the net cooling contribution to the ML heat budget visible south of the ITCZ diagonal (Figure 10A) can only be due to the fraction of the solar flux that penetrates below the ML.”

Probably not a substantial claim: may not pass S1 (asserted), S3 (load-bearing). May combine two claims.

Santos et al. suggest that if upwelling is persistent throughout the year, with a peak in autumn and spring between 21 and 32°N, it would be restricted to winter-spring within the 12-20°N latitude band.

“For example, Santos et al. [24], using a temperature-based estimate suggest that if the upwelling is persistent throughout the year, with a peak in autumn and spring, between 21 and 32 • N, it would in contrast be restricted to winter-spring within the 12 • and 20 • N latitude band.”

• cites [24] Santos, 2005, Decadal changes in the Canary upwelling system as revealed by satellite observations: their impact on productivity, J Mar Res sourceNot checked — no full text of the source

Probably not a substantial claim: may not pass S3 (load-bearing). May combine two claims.

Carton and Zhou ocean model sensitivity experiments show that air-sea flux and wind stress forcing are of comparable importance away from the continent, whereas within a few degrees of the African coasts the meridional stress becomes the main forcing.

“Carton and Zhou [20] ocean model sensitivity experiments show that air-sea flux and wind stress forcing are of comparable importance away from the continent, whereas within a few degrees of the African coasts, the meridional stress becomes the main forcing.”

• cites [20] Carton, 1997, Annual cycle of sea surface temperature in the tropical Atlantic Ocean, J Geophys Res sourceNot checked — no full text of the source

May combine two claims.

Kz is more homogeneous zonally and exhibits higher values far from the continent, possibly due to weaker stratification at this period that is favorable to turbulence.

“K z is more homogeneous zonally and exhibits higher values far from the continent, possibly due to the weaker stratification at this period that is favorable to turbulence.”

Probably not a substantial claim: may not pass S3 (load-bearing). May combine two claims.

The grouped ocean terms were checked individually relative to the others and are discussed separately when significant.

“These group components have been checked individually relative to the others, and are discussed separately when they are significant.”

Classified as probably not a substantial claim.

Important limitations in the present study are due to the scarcity of in-situ observations.

“Important limitations in the present study are due to the scarcity of in-situ observations.”

May combine two claims.

The ocean processes cooling effect is not a driver of the change from net positive to net negative trend since it entered a decreasing phase around this period, explained by the attenuation of the trade winds and associated Ekman pumping.

“It is not a driver since it entered a decreasing phase around this period, explained by the attenuation of the trade winds (Figure 4) and associated Ekman pumping (Figure 2).”

May combine two claims.

Model results are limited by inherent errors due to the relatively low horizontal and vertical resolution near the coast, and uncertainties in air-sea fluxes.

“Our model results are limited by inherent errors due to the relatively low horizontal and vertical resolution near the coast, and uncertainties in air-sea fluxes.”

Probably not a substantial claim: may not pass S3 (load-bearing).

This clarifies the results from Yamagata and Iizuka [7], pertaining to the thermocline and not to the ML, which explained the decrease in heat content by horizontal and vertical divergence of the heat transport in all GD.

“It clarifies the results from Yamagata and Iizuka [7], pertaining to the thermocline and not to the ML, which explained the decrease in heat content by horizontal and vertical divergence of the heat transport in all GD.”

• cites Yamagata and Iizuka [7] Yamagata, 1995, Simulation of the tropical thermal domes in the Atlantic: a seasonal cycle, J Phys Oceanogr sourceNot checked — no full text of the source