Although the demolitions continue unabated in the centuries-old Freedmen’s town, residents in the Tenth Street Historic District got at least a little bit of good news Thursday morning as they gathered in one of the many vacant — yet freshly mowed — lots for an announcement.
It’s an area that hasn’t seen a lot of great news — since it was given its landmark designation by the city in 1993, 72 homes of 260 in the historic neighborhood have been torn down. The community formed the Tenth Street Residential Association to take on the city, and has filed suit to stop the demolitions and to shore up the historic protections it is supposed to have.
But Thursday, the neighborhood got a bit of a boost in its quest to improve its lot, as the National Trust for Historic Preservation announced that it had named the district to its 32nd annual list of America’s 11 Most Endangered Historic Places.
“This list has called attention to hundreds of threatened sites and places across the country and has helped galvanize communities to defend them,” Meg Lousteau, associate field director of the Trust’s Houston field office, told those gathered, adding that the list has been so effective in the past that fewer than five percent of the sites named to it have been lost.
“And now we’re here in the Tenth Street Historic District, a neighborhood that has been ravaged by disinvestment, neglect, and rampant demolition,” Lousteau said.
The news means that the district will now at least have more attention and muscle behind its efforts. In the past, that support from the Trust has included everything from legal assistance, grassroots advocacy campaigns, and publicity in the organization’s magazine and website.
“We are on sacred land … cultivated by those who were enslaved, and then were no longer enslaved,” said Demetria McCain, President Inclusive Communities Project. The ICP has been working with residents on numerous issues regarding the fight to stop the demolition and improve infrastructure in the community.
Tenth Street has been home to Black Dallasites for more than a century, and is one of the few remaining intact Freedmen’s towns in the nation. Settled by freed slaves after the Civil War, many of those families continue to hold on to the homes and land their newly-freed ancestors were undoubtedly proud to own.
The neighborhood’s genesis was in the 1880s, as it took shape south of the Trinity River in one of the few spots the Black community could own land. By now, the neighborhood would be considered the northeastern edge of Oak Cliff, bounded by Interstate 35, East Eighth Street, and Clarendon Drive.
In 1944, the city designated the Tenth Street community a “Negro only” area. In 1947, the neighborhood was zoned for duplex and single-family residential use only. As desegregation became a drumbeat in the 1960s, construction of Interstate 35 was routed through the neighborhood, severing the majority-Black neighborhood from then predominantly white Oak Cliff, but it demolished homes and businesses in its path.
The decade also saw another hit to the neighborhood — a zoning change that made the single family homes in Tenth Street non-conforming uses. The city had the chance to fix the zoning issues that changed the fabric of Tenth Street in 1984, when a new set of planning policies presumably prioritized stabilizing neighborhoods and quality of life. Those new policies also were enacted to protect residential neighborhoods.
But that wasn’t the case for Tenth Street. Since its zoning had been changed to nonconforming use in the 60s, it was instead named a Future Growth Corridor, meaning that it could now be home to commercial, regional retail, industrial manufacturing, and townhomes — a far cry from the residential zoning of its neighbors.
“If you want to see neighborhood inequity in action, you found it,” said Inclusive Communities’ Planning and Community outreach director Jennifer Rangel, adding that compared to white historic districts, abandoned homes in black historic neighborhoods are more likely to fall prey to demolition by the city.
“Despite the Inclusive Communities’ requests to the city council to amend or repeal the ordinance, they have not done so,” Rangel said. “The City of Dallas has a duty to affirmatively further fair housing. It must repeal this ordinance that singles out and affects Black historic districts and its residents.”
How do all these homes in a historic district get demolished? Basically, thanks to a city code that allows for the demolition of homes less than 3,000 square feet, regardless of whether they’re in a historic district or not. Dallas City Code 51A-4.501(i) allows the city to remove the protections generally afforded historic homes if they fall under that allowed 3,000 square feet.
Compared to the 72 demolitions from 1993 to 2017 in Tenth Street, substantially fewer demolitions occurred in predominately white historic neighborhoods during the same time, with five demolitions happening in Peak’s Addition; four demolitions happening in Winnetka Heights and Munger Place; three in Junius Heights; two each in Swiss Avenue and State-Thomas; one in South Boulevard-Park Row; and none in Lake Cliff Park.
“Understand that in the City of Dallas, on the corner of Worth Street and Fitzhugh, you’ll find a very large dilapidated, old building in a white historic district,” McCain said. “It’s over 3,000 square feet. However, it still stands, and if you go by there today, it’s being renovated. Why is that? Because it’s in a white historic district.”
“I invite you to drive by Worth and Fitzhugh, and you can see, no matter how dilapidated, many of these structures actually can be saved.”
Patricia Cox, Tenth Street Residential Association president, has watched her neighborhood be torn down bit by bit for years now.
“We started seeing our homes disappear,” she said. “We started getting new neighbors who wanted to refurbish their homes, but they were on the demolition list.”
So the residents coalesced to become an association aimed at addressing the rampant demolition and to hopefully wrest some sort of stay of execution from the city.
“We tried to work with the city — still trying to work with the city, to no advantage,” she said. “So we’re still here, fighting a battle, and we will be.”
Residents told of the history of the neighborhood — what was here when the community wasn’t cut off from the rest of the city by I-35, and then builder and developer Larry Johnson stepped up to speak. Johnson said he’s been working to save and renovate homes in the district for some time, and has attended meetings with the city — with Mayor Mike Rawlings and people in the Mayor’s office, as well as landmark commission and pretty much any city office that could slow the piecemeal — yet devastating — bulldozing of the freedman’s town.
Johnson and his sons routinely make sure the now vacant lots, as well as the outward facing properties in the neighborhood are mowed regularly. Is also helping a property owner nearby refurbish their house because, he said, they “want Tenth Street to be beautiful.”
Keeping the community’s history intact, he said, is vital to Black Dallas, and its children.
“My other personal fight to save Tenth Street is steeped in knowing that people that look like me, we perish for a lack of knowledge,” he said. “The reality is that a lot of the things that we do, we do because we don’t know where we’ve come from. We don’t know about the accomplishments of people that look just like that.”
“Tenth Sreet is the answer to that issue,” he said, to applause. “Tenth Street was settled by freed slaves, that when an emancipated, had nothing, but according to records, were able to buy land within three to five years of emancipation.”
His admiration of the people who eked out first survival, and then thrived, on the land the crowd stood on Thursday was palpable.
“They didn’t act out of desperation. They didn’t let hard times get the best of them,” he said. “They rose above the situation, they did not let their circumstance dictate their outcome and they did the best that they could and they built a beautiful community.”
“And that’s one of the main reasons I’m fighting so hard.”


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|Cash at bank and in hand||1|
|CAPITAL AND RESERVES||2015|
SEA CITY INVESTMENTS LIMITED has been working since 12/15/2014. The current status of the business is Active SEA CITY INVESTMENTS LIMITED located on 16 SOUTH END, CROYDON, SURREY, UNITED KINGDOM, CR0 1DNDirector Nicholas Benjamin Anthony is known as a Director of the company. Director Marksohn Beau Adam is known as a Director of the company. "Buying and selling of own real estate" is a known activity of the company.

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During the last decade, many studies have focused on interannual climate variability associated with the El Niño–Southern Oscillation (ENSO). Progress has been made in understanding and simulating the coupled tropical ocean–atmosphere system by using models of varying complexity (e.g., Philander 1990; McCreary and Anderson 1991; Neelin et al. 1998). Four conceptual oscillator models have been proposed to interpret ENSO-like oscillations: 1) the delayed oscillator (Suarez and Schopf 1988; Graham and White 1988; Battisti and Hirst 1989; Cane et al. 1990); 2) the western Pacific oscillator (Weisberg and Wang 1997b; Wang et al. 1999b); 3) the recharge–discharge oscillator (Jin 1997a,b); 4) the advective–reflective oscillator (Picaut et al. 1997).
A mechanism for the oscillatory nature of ENSO was originally proposed by McCreary (1983), based on the reflection of subtropical oceanic upwelling Rossby waves at the western boundary. Suarez and Schopf (1988) introduced the conceptual delayed oscillator (with an ordinary differential delay equation) as a candidate mechanism for ENSO, by considering the effects of equatorially trapped oceanic waves propagating in a closed basin through a delay term. Based on the coupled ocean–atmosphere model of Zebiak and Cane (1987), Battisti and Hirst (1989) formulated and derived a version of the Suarez and Schopf (1988) conceptual delayed oscillator model and argued that this delayed oscillator model could account for important aspects of the numerical model of Zebiak and Cane (1987). Graham and White (1988) presented observational evidence of off-equatorial Rossby waves and their reflection at the western boundary and then empirically constructed a conceptual oscillator model for ENSO. As shown in McCreary and Anderson (1991), the conceptual equations of the Graham and White model can be reduced to a single equation that has similar form to the delayed oscillator [also see the comments of Neelin et al. (1998)]. The conceptual delayed oscillator model is represented by a single ordinary differential delay equation with both positive and negative feedbacks. The positive feedback is represented by local ocean–atmosphere coupling in the equatorial eastern Pacific. The delayed negative feedback is represented by free Rossby waves generated in the eastern Pacific coupling region that propagate to and reflect from the western boundary, returning as Kelvin waves to reverse the anomalies in the eastern Pacific coupling region. Thus, the coupled ocean–atmosphere system oscillates on interannual timescales.
Consistent with observations (e.g., Weisberg and Wang 1997a; Mayer and Weisberg 1998; Wang et al. 1999b), Weisberg and Wang (1997b) developed a conceptual western Pacific oscillator model for ENSO. This model emphasizes the role of the western Pacific in ENSO, which has been overlooked in the delayed oscillator. In particular, off-equatorial sea surface temperature (SST) and sea level pressure (SLP) anomalies in the western Pacific induce equatorial western Pacific wind anomalies that affect the evolution of ENSO. The western Pacific oscillator model considers the thermocline depth anomalies in the equatorial eastern Pacific, the equatorial zonal wind stress anomalies in both the central Pacific and the western Pacific, and the off-equatorial thermocline depth anomalies in the western Pacific. Arguing from the vantage point of a Gill (1980) atmosphere, condensation heating due to convection in the equatorial central Pacific (Deser and Wallace 1990;Zebiak 1990) induces a pair of off-equatorial cyclones with westerly wind anomalies on the equator. These equatorial westerly wind anomalies act to deepen the thermocline and increase SST in the equatorial eastern Pacific, thereby providing a positive feedback for anomaly growth. On the other hand, the off-equatorial cyclones raise the thermocline there via Ekman pumping. Thus, a shallow off-equatorial thermocline anomaly expands over the western Pacific leading to a decrease in SST and an increase in SLP in the off-equatorial western Pacific (e.g., Wang et al. 1999b). During the mature phase of El Niño, this off-equatorial high SLP initiates equatorial easterly wind anomalies in the western Pacific. These equatorial easterly wind anomalies cause upwelling and cooling that proceed eastward as a forced ocean response providing a negative feedback for the coupled ocean–atmosphere system to oscillate.
Jin (1997a,b) proposed a recharge–discharge oscillator model for ENSO. This model considers SST anomalies in the equatorial eastern Pacific and thermocline depth anomalies in the equatorial western Pacific. Although the physics of this oscillator seems to not be so obvious from its mathematical form, he claimed that it represents the discharge and recharge of equatorial heat content. He argued that, during the warm phase of ENSO, the divergence of Sverdrup transport associated with equatorial central Pacific westerly wind anomalies and equatorial eastern Pacific warm SST anomalies results in the discharge of equatorial heat content. The discharge of equatorial heat content leads to a transition phase in which the entire equatorial Pacific thermocline depth is anomalously shallow due to the discharge of equatorial heat content. This anomalous shallow thermocline at the transition phase allows anomalous cold waters to be pumped into the surface layer by climatological upwelling and then leads to the cold phase. The converse occurs during the cold phase of ENSO. It is the recharge–discharge process that makes the coupled ocean–atmosphere system oscillate on interannual timescales.
All of the above oscillator models are represented by simple and heuristic ordinary differential equations. Picaut et al. (1997) also proposed a conceptual model for ENSO by emphasizing the importance of zonal displacements of the western Pacific warm pool and wave reflection at both western and eastern boundaries, without a set of simple and heuristic equations. Using a linear wind-forced ocean numerical model that was restricted to the zonal current of the first baroclinic Kelvin and first meridional Rossby waves, they showed an interannual oscillation with specified model parameters. They argued that anomalous zonal currents associated with equatorial wave reflection at both the western and eastern boundaries and mean zonal currents provide negative feedbacks for their model to oscillate.
With the different conceptual oscillator models capable of producing ENSO-like oscillations, more than one may operate in nature. However, a conceptual oscillator model including the different oscillator physics discussed above does not exist. The purpose of this paper is to formulate and derive a unified conceptual oscillator model from which the different oscillator models can be extracted as special cases. The paper is organized as follows. In section 2, observations of eastern and western Pacific interannual anomaly patterns are reviewed to better understand conceptual oscillator models. In section 3, a unified conceptual oscillator model is formulated and derived, and its relationships to other oscillators are discussed. Analyses of linear instability for the unified oscillator are performed in section 4. Summary and discussion are given in section 5.
2. Observations of ENSO eastern and western Pacific anomaly patterns
To help us better understand the different conceptual oscillator models for ENSO, we first review observations showing eastern and western Pacific interannual anomaly patterns and their relationships. Rasmusson and Carpenter (1982) gave a comprehensive description of a composite El Niño using the surface wind and SST data from 1949 to 1976, and Rasmusson and Wallace (1983) presented outgoing longwave radiation (OLR) anomalies during the 1982–83 El Niño. These studies focused on ENSO eastern Pacific anomaly patterns since interannual anomalies in the eastern Pacific are large. During the warm phase of ENSO, warm SST and low SLP anomalies are found in the equatorial eastern Pacific, and low OLR anomalies are in the equatorial central Pacific. Associated with the distributions of SST, SLP, and OLR anomalies, zonal wind anomalies are westerly in the equatorial central Pacific.
Recently, Wang et al. (1999b) emphasized ENSO western Pacific patterns in addition to eastern Pacific patterns, using the Comprehensive Ocean–Atmosphere Dataset (COADS) data from January 1950 to December 1992 (Woodruff et al. 1987) and the OLR data from January 1974 to December 1992 (obtained from the NOAA–NCEP). Based on these data, the horizontal structures of the tropical Pacific SST, OLR, SLP, and surface wind anomalies for a composite El Niño were calculated as shown in Fig. 1. The El Niño composite was formed by taking the average December anomalies for 1957, 1965, 1972, 1982, 1986, and 1991. During the peak of El Niño, when the warmest SST anomalies are in the equatorial eastern Pacific, the coldest SST anomalies are located to the north and south of the equator in the western Pacific, instead of on the equator. Since atmospheric convection over the western Pacific warm pool shifts into the equatorial central Pacific during the warm phase of ENSO, the region of the lowest OLR anomalies is located to the west of the warmest SST anomalies. Like the relative position between the SST and OLR anomalies in the equatorial eastern and central Pacific, in the western Pacific the off-equatorial region of highest OLR anomalies is positioned west of the off-equatorial region of coldest SST anomalies. The off-equatorial western Pacific cold SST anomalies are also accompanied by off-equatorial western Pacific high SLP anomalies. As a result of off-equatorial high SLP anomalies, equatorially convergent winds are generated that turn anticyclonically to equatorial easterly wind anomalies over the western Pacific, as observed in Fig. 1d. Thus, during the mature phase of El Niño, the equatorial eastern Pacific shows warm SST and low SLP anomalies, and the equatorial central Pacific shows low OLR anomalies, while the off-equatorial western Pacific shows cold SST and high SLP anomalies, and the off-equatorial far western Pacific shows high OLR anomalies. Associated with these SST, SLP, and OLR anomaly patterns are equatorial westerly wind anomalies in the central Pacific and equatorial easterly wind anomalies in the western Pacific. The nearly out-of-phase behavior between the eastern and western tropical Pacific is also observed during the cold phase of ENSO, but with anomalies of opposite sign.
For the purpose of comparison between eastern and western Pacific interannual variability, Wang et al. (1999b) defined two new regional ENSO indices in addition to the conventional ENSO indices, consistent with observations in Fig. 1. The conventional eastern and central Pacific ENSO indices are: Niño-1 over 10°–5°S, 90°–80°W; Niño-2 over 5°S–0°, 90°–80°W; Niño-3 over 5°S–5°N, 150°–90°W; and Niño-4 over 5°S–5°N, 160°E–150°W. The new western Pacific ENSO indices are: Niño-5 over 5°S–5°N, 120°–140°E and Niño-6 over 8°–16°N, 140°–160°E. Comparisons of the SST anomalies between the Niño-3 and Niño-6 regions, and the zonal wind anomalies between the Niño-4 and Niño-5 regions are shown in Figs. 2a and 2b, respectively. The SST anomalies in the Niño-3 region are out-of-phase with those in the Niño-6 region. That is, the warm (cold) SST anomalies in the equatorial eastern Pacific during El Niño (La Niña) are accompanied by the cold (warm) SST anomalies in the off-equatorial western Pacific. Similarly, zonal wind anomalies in the central Pacific tend to be out-of-phase with those in the western Pacific. During the mature warm (cold) phase of ENSO, equatorial westerly (easterly) wind anomalies in the central Pacific are accompanied by equatorial easterly (westerly) wind anomalies in the western Pacific.
The 1997–98 El Niño is no exception, also showing the western Pacific anomaly patterns. Wang and Weisberg (2000) described how off-equatorial western Pacific SLP anomalies evolve and how they produce equatorial wind anomalies in the western Pacific. Time–longitude plots of SST and zonal wind anomalies along the equator during the 1997–98 El Niño are show in Fig. 3. Equatorial westerly wind anomalies appear over the far western Pacific in November/December 1996. The continuous westerly anomalies and their eastward penetration are associated with an initial warming in January/February 1997 in the central Pacific. The warming also appears in March 1997 along the South American coast. The warm SST anomalies in the equatorial central Pacific propagate eastward, whereas the warm SST anomalies in the far eastern Pacific grow and spread westward. In June 1997, the eastward propagating and westward spreading SST anomalies merge together, forming a large-scale warming in the equatorial central and eastern Pacific. Then, the warm SST anomalies grow but do not propagate. Equatorial easterly wind anomalies over the far western Pacific also lead the decay phase of the 1997–98 El Niño. Like the equatorial westerly wind anomalies that initiate the early warming (e.g., Wyrtki 1975; McCreary 1976; Busalacchi and O’Brien 1981; Philander 1981), the equatorial easterly wind anomalies in the western Pacific may force upwelling Kelvin waves that propagate eastward (Tang and Weisberg 1984; Philander 1985) and help facilitate the 1997–98 El Niño decay. Both the onset and decay phases of the 1997–98 El Niño seem to relate to wind anomalies in the western Pacific.
The western Pacific anomaly patterns are robust features of ENSO, independent of datasets. The western Pacific anomaly patterns also appear in other datasets and in other studies (e.g., Rasmusson and Carpenter 1982; Rasmusson and Wallace 1983; Graham and White 1988, 1991; White et al. 1987, 1989; Kessler 1990; Chao and Philander 1993; Delcroix et al. 1994; Mestas-Nuñez and Enfield 2001), but these patterns were not emphasized, probably due to the relatively small magnitude of SST anomalies when compared with those from the eastern Pacific patterns. However, the small SST anomalies in the off-equatorial western Pacific are sufficient to produce atmospheric responses of comparable amplitude to those in the equatorial eastern Pacific, due to the mean state of atmospheric convergence there associated with the western Pacific warm pool (Wang et al. 1999b; Wang 2000).
3. A unified oscillator model
In this section we first formulate and derive a unified oscillator model. We then discuss the relationships of this unified oscillator with the delayed oscillator, the western Pacific oscillator, the recharge–discharge oscillator, and the advective–reflective oscillator, and show how the different oscillators can be extracted as special cases of this unified oscillator model. The behavior of the unified oscillator model is also discussed.
a. Formulation and derivation of unified oscillator model
b. Relations to previous oscillator models
In this section, we will show that the ENSO conceptual models of the delayed oscillator, the western Pacific oscillator, and the recharge–discharge oscillator can be extracted as special cases of the unified oscillator model of Eqs. (7), (10), (13), and (14) by further simplifications and assumptions. The relationships between the unified oscillator and the advective–reflective oscillator are also discussed.
1) The delayed oscillator
2) The western Pacific oscillator
During the warm phase of ENSO, with atmospheric convection extending eastward into the Niño-4 region, westerly wind anomalies are maximum there, and which increase the Niño-3 SST anomalies as represented by the first term in Eq. (18a). During the mature phase of El Niño, equatorial easterly wind anomalies are produced in the western Pacific. Easterly wind anomalies force eastward propagating upwelling Kelvin waves to affect the Niño-3 SST anomalies. The contribution of the wind-forced Kelvin waves is represented by the second term in Eq. (18a). The corollary off-equatorial response to the same process that causes central Pacific equatorial westerly wind anomalies is off-equatorial Rossby waves induced by off-equatorial wind stress curl. Westward propagating Rossby waves raise the thermocline in the Niño-6 region, as represented by Eq. (18b). The coupled system does not necessarily involve off-equatorial Rossby wave reflection at the western boundary. This is consistent with the conclusions of Battisti (1989), who argued that reflection of off-equatorial Rossby waves (outside of 8° lat) at the western boundary does not contribute to ENSO. Equation (18c) parameterizes the linear relationship between the Niño-4 zonal wind stress anomalies and the Niño-3 SST anomalies. Equation (18d) relates the initiation of the Niño-5 easterly wind anomalies to the Niño-6 thermocline depth variations.
3) The recharge–discharge oscillator
The mathematical form of Eq. (21) is the same as the recharge–discharge oscillator of Jin (1997a), but its interpretation may be different. Herein, h represents western Pacific off-equatorial thermocline depth anomalies, whereas Jin interpreted it as western Pacific equatorial thermocline depth anomalies. In the formulation of the recharge–discharge oscillator model, Jin (1997b) used a two-strip (one for equatorial strip and another for off-equatorial strip) approximation to the ocean dynamics. The equation controlling thermocline depth variations in the off-equtorial strip [his Eq. (2.5)] is the same equation as our Eq. (8). [Note that Eq. (8) is not valid in the equatorial regions.] The finite difference form of this equation also represents off-equatorial thermocline depth variations [see his Eq. (3.2b)]. He further assumed that off-equatorial thermocline depth anomalies are linearly related to equatorial thermocline depth anomalies by wave reflection at the western boundary [note that, like the delayed oscillator, the effect of equatorial wave reflection at the western boundary has already been considered in the unified oscillator model as in the second term of Eq. (7)]. Therefore, the equation that controls thermocline depth variations in his recharge–discharge oscillator model becomes one associated with equatorial western Pacific thermocline depth anomalies rather than off-equatorial western Pacific thermocline depth anomalies. However, observations show that maximum interannual SST (e.g., Figs. 1 and 2), thermocline depth (White et al. 1987, 1989; Kessler 1990), and sea level (Delcroix et al. 1994; Busalacchi 1996, personal communication) variations are in the western Pacific off-equatorial region. Therefore, this raises a question how to interpret the mathematical form of the recharge–discharge oscillator. If we consider thermocline depth variations as being in the off-equatorial western Pacific region, the recharge–discharge oscillator can be exactly reduced from the unified oscillator.
4) The advective–reflective oscillator
Picaut et al. (1996) found that zonal displacement of the oceanic convergence zone at the eastern edge of the western Pacific warm pool is in phase with the Southern Oscillation index. Based on this finding and the study of Picaut and Delcroix (1995) regarding wave reflection, Picaut et al. (1997) proposed a conceptual advective–reflective oscillator model for ENSO. In this conceptual model, they emphasize a positive feedback of zonal currents that advect the western Pacific warm pool toward the east. Three negative feedbacks tending to push the warm pool back to its original position of the western Pacific are anomalous zonal current associated with wave reflection at the western boundary, anomalous zonal current associated with wave reflection at the eastern boundary, and mean zonal current converging at the eastern edge of the warm pool. Using a linear wind-forced ocean numerical model (instead of simple and heuristic equations like the other oscillators) that emphasizes the above physics, they showed an interannual oscillation. We herein discuss how the physics of the advective–reflective oscillator can be summarized into the unified oscillator and its possible relationships with the unified oscillator.
Picaut et al. (1997) argued that equatorial westerly wind anomalies in the central Pacific induce eastward anomalous zonal currents that advect the western Pacific warm pool eastward. The eastward warm pool displacement decreases the east–west SST gradient that further strengthens the equatorial westerly wind anomalies. This positive feedback leads El Niño to a growth phase. In terms of the unified oscillator model, the positive feedback of zonal advection is included in the first term of Eq. (7) (i.e., in aτ1). In the SST equation of Eq. (1), zonal advection of the mean zonal SST gradient by the anomalous zonal current is u∂
At the same time, equatorial westerly wind anomalies in the central Pacific produce upwelling Rossby waves and downwelling Kelvin waves that propagate westward and eastward, respectively. The upwelling Rossby waves reflect to upwelling Kelvin waves after they reach the western boundary. Since the upwelling Kelvin waves have westward zonal currents, they tend to push the warm pool back to its original position of the western Pacific. Although the physics of this negative feedback is not exactly the same as that of the delayed oscillator, it may be included in the term of −b1τ1(t − η) in Eq. (7).
Picaut et al. (1997) also argued that the mean zonal current plays a negative feedback since it may help to push the warm pool in the central Pacific during the warm phase of ENSO back to the western Pacific. For their model to oscillate, they had to use the mean zonal current stronger than observed mean zonal current. This may be because other negative feedbacks are also operating in the coupled ocean–atmosphere system. For example, the negative feedback of easterly wind-forced ocean responses in the western Pacific cannot be ignored. In nature, the combination of different negative feedbacks makes the coupled system switch from a warm (cold) phase to a cold (warm) phase. Notice that zonal advection of the anomalous zonal SST gradient by the mean zonal current is also in Eq. (1) from which the unified oscillator is formulated and derived.
c. Numerical solutions
The unified oscillator model can be solved numerically by using the predictor-corrector method of the Adams–Bashforth–Moulton scheme (e.g., Press et al. 1990). Since the unified oscillator model can be reduced to different oscillator models, the model parameters are chosen to be consistent with those in the delayed oscillator model of Battisti and Hirst (1989) and in the western Pacific oscillator of Weisberg and Wang (1997b). Neglecting the role of the western Pacific (b2 = 0), the unified oscillator model reduces to delayed oscillator models. Choosing the model parameters of a = 1.5 × 102 °C m2 N−1 yr−1, b1 = 2.5 × 102 °C m2 N−1 yr−1, d = 3.6 × 10−2 °C−1 N m−2 yr−1, ε = 1.2 °C−2 yr−1, Rτ1 = 2.0 yr−1, and η = 150 days, Eq. (17) shows that this set of parameters is in the range of the delayed oscillator of Battisti and Hirst (1989). They argued that it represents the coupled ocean–atmosphere system in the equatorial Pacific. With these model parameters, the solutions of the one and two variable delayed oscillators [Eqs. (17) and (15)] are shown in Figs. 4 and 5, respectively. Both of the solutions oscillate on interannual timescales. The one variable delayed oscillator shows a shorter oscillatory period and a larger oscillatory amplitude.
The solution of the western Pacific oscillator (b1 = 0) of Eq. (18) is shown in Fig. 6, with the model parameters: a = 1.5 × 102 °C m2 N−1 yr−1, b2 = 7.5 × 102 °C m2 N−1 yr−1, c = 1.5 × 103 m3 N−1 yr−1, d = 3.6 × 10−2 °C−1 N m−2 yr−1, e = 3.0 × 10−3 N m−3 yr−1, ε = 1.2 °C−2 yr−1, Rh = 5.0 yr−1, Rτ1 = Rτ2 = 2.0 yr−1, δ = 30 days, and λ = 180 days. These values of the model parameters are chosen to be close to those in Weisberg and Wang (1997b). Since it takes approximately a month for a Kelvin wave to propagate from the western Pacific to the east-central Pacific, δ is set to 30 days. The off-equatorial Rossby wave speed cr =
Next, we see the model solution of the unified oscillator (b1 ≠ 0 and b2 ≠ 0). With the parameters of Figs. 5 and 6, in which both the delayed and western Pacific oscillator models can oscillate, Fig. 7 shows the solution of the unified oscillator model of Eqs. (7), (10), (13), and (14). The model also oscillates on interannual timescales. Comparisons of Fig. 7 with Figs. 5 and 6 show that, for the model parameters used, oscillatory amplitude of the unified oscillator is larger than that for the delayed oscillator, and oscillatory period is shorter than that for the western Pacific oscillator. Note that the delayed version of the recharge–discharge oscillator model of Eq. (20) also can oscillate by using the model parameters above (not shown).
The effect of wave reflection at the eastern boundary of the advective–reflective oscillator in the unified oscillator can be seen by solving Eqs. (22), (10), (13), and (14). Since it takes about three months for a Kelvin wave in the equatorial central Pacific to propagate to the eastern boundary and then to reflect back to the equatorial eastern Pacific, we choose μ = 90 days. With μ = 90 days and b3 = b1 (assume the same contribution from the western and eastern boundaries), Fig. 8 shows the solution of Eqs. (22), (10), (13), and (14). Comparisons with Fig. 7 show that the inclusion of the negative feedback of wave reflection at the eastern boundary decreases the oscillatory period. It also reduces the oscillatory amplitudes (notice a scale difference between Figs. 7 and 8).
The cubic damping term is added to Eq. (7) for limiting anomaly growth. To assess its effects on oscillatory behavior of the coupled system, Fig. 9 shows the dependence of both period and amplitude of the unified oscillator model upon the damping coefficient ε. The period of the oscillations is independent of ε, whereas the amplitude of the oscillations is increased with decreasing ε. The cubic damping does not affect oscillatory behavior, but it limits anomaly growth.
Is the result of the unified oscillator model consistent with more complicated ocean models? To address this question, the oceanic component of the Lamont coupled ocean–atmosphere model is used. Since the Lamont coupled model cannot simulate equatorial wind anomalies in the western Pacific very well, we use the Florida State University (FSU) pseudo wind stress to force the ocean model. Two experiments have been performed: one is with full wind forcing in the tropical Pacific and the other is with western Pacific winds removed. The results of model Niño-3 thermocline anomalies for the 1982–83 and 1997–98 El Niños are shown in Figs. 10a and 10b, respectively. The Niño-3 thermocline anomalies for the experiment with full wind forcing in the tropical Pacific are larger than those for the experiment without western Pacific winds. This is consistent with the result of the unified oscillator model in that considering the wind-forced wave contribution in the western Pacific the oscillatory amplitude is larger than that for the delayed oscillator. The experiment without western Pacific winds also shows a delay for the onset of the 1982–83 and 1997–98 El Niños (with an approximate 3-month delay).
4. Analyses of linear instability
The dispersion relationship of Eq. (25) has many parameters, so linear instability exists in a multidimensional parameter space. The parameters a, d, and e are related to positive feedbacks. With other parameters as in Fig. 7, growth rate σr and frequency σi dependences on these three parameters are shown in Fig. 11. There is one unstable oscillatory mode for values of a smaller than 340.0°C m2 N−1 yr−1. The frequency is decreased with increasing a, whereas the growth rate is increased with a. As a is increased to values larger than 340.0°C m2 N−1 yr−1, one oscillatory mode splits into two nonoscillatory modes (σi = 0). The growth rate is increased with a for one mode and is decreased for another one. This behavior is similar to findings of Wakata and Sarachik (1991) and Jin (1997a). These results suggest that sufficiently strong positive ocean–atmosphere interactions may not allow the coupled ocean–atmosphere system to oscillate. The parameter d shows a similar result. As d is sufficiently large, the unstable oscillatory mode splits into two nonoscillatory modes. The dependence of frequency and growth rate on the positive feedback parameter e is relatively simple. Both frequency and growth rate are increased with increasing e.
The parameters b1, b2, and c are related to negative feedbacks of the coupled system. These parameters are associated with the effect of equatorial wave reflection at the western boundary on the Niño-3 SST anomalies, the effect of equatorial western Pacific wind-forced wave on the Niño-3 SST anomalies, and the effect of off-equatorial wind stress curl-induced Rossby waves on the Niño-6 thermocline depth anomalies, respectively. Increasing these processes makes coupled systems easily switch from a warm (cold) phase to a cold (warm) phase. Therefore, the period of oscillation is expected to be decreased with an increase in the strength of these processes. Frequency and growth rate dependence on these parameters are shown Fig. 12. Both frequency and growth rate are increased with increasing b1, b2, and c. However, frequency is more sensitive to b1 than to b2 and c. Figures 12b and 12c show that the period of the unified oscillator model does not change much with the variations of b2 and c. This explains why adding the negative feedback of the equatorial wind-forced response in the western Pacific has little effect on the period of the oscillations in section 3c. Figure 12 also shows that when b1 is decreased from the standard value of 2.5 × 102 °C m2 N−1 yr−1 to zero, the growth rate does not change much. However, when b2 is decreased from the standard value of 7.5 × 102 °C m2 N−1 yr−1 to zero, the growth rate is reduced to half. This is also consistent with the result in section 3c in that the amplitudes of the unified oscillator remain as those of the western Pacific oscillator (since removing the negative feedback of b1 does not change the growth rate of the system).
The parameters Rh, Rτ1, and Rτ2 are related to linear damping terms in the equations controlling variations of h, τ1, and τ2, respectively. Figure 13 shows growth rate and frequency dependence on these parameters. The growth rate is decreased with increasing Rh, Rτ1, and Rτ2 since their effects on the coupled system are damping. The frequency is not so sensitive to Rh, Rτ1, and Rτ2. Like the nonlinear damping coefficient ε shown in Fig. 9, the linear damping coefficients Rh, Rτ1, and Rτ2 do not have a large effect on the period of oscillations for the unified oscillator model.
There are three delay parameters η, δ, and λ, which are related to three negative feedbacks in the coupled system. Increasing these parameters increases the time for negative feedbacks to switch the coupled system from the warm (cold) phase to the cold (warm) phase, and therefore increases the period of the model oscillations. Growth rate and frequency dependence on these parameters are shown in Fig. 14. The frequency is decreased with η, δ, and λ. The growth rate is increased with η for small values of η and it then remains almost constant, whereas the growth rate is decreased with increasing δ and λ.
5. Summary and discussion
A unified conceptual oscillator model for ENSO is formulated and derived from the dynamics and thermodynamics of the coupled ocean–atmosphere system. Since ENSO is observed to show both eastern and western Pacific anomaly patterns, this oscillator model is constructed to consider SST anomalies in the Niño-3 region, equatorial zonal wind stress anomalies in the Niño-4 region, thermocline depth anomalies in the Niño-6 region, and equatorial zonal wind stress anomalies in the Niño-5 region. If the role of western Pacific wind-forced response in eastern Pacific SST anomalies is neglected, the Niño-6 thermocline and Niño-5 wind stress anomalies are decoupled from the coupled system, and the unified oscillator reduces to the delayed oscillator. Neglecting equatorial wave reflection at the western boundary reduces the unified oscillator to the western Pacific oscillator. If we assume that the Niño-4 and Niño-5 zonal wind stress anomalies are directly proportional to the Niño-3 SST and Niño-6 thermocline anomalies, respectively, the unified oscillator mathematically reduces to the recharge–discharge oscillator. Most of the physics of the advective–reflective oscillator are implicitly included in the unified oscillator, and the negative feedback of wave reflection at the eastern boundary is added to the unified oscillator. With the model parameters chosen to be consistent with those of previous oscillator models, the unified oscillator model oscillates on interannual timescales. For the model parameters used, the western Pacific wind-forced response makes the coupled system oscillate with a larger amplitude, consistent with results from an intermediate ocean model.
All of the conceptual oscillator models have a positive ocean–atmosphere feedback that occurs in the equatorial eastern and central Pacific. Each, however, has different negative feedbacks that turn the warm (cold) phase into the cold (warm) phase. In the delayed oscillator, free Rossby waves generated in the equatorial eastern Pacific propagate westward and reflect from the western boundary as Kelvin waves. Since thermocline depth anomalies for the returning Kelvin waves have signs opposite to those in the equatorial eastern Pacific, these provide a negative feedback for the coupled ocean–atmosphere system to oscillate. In the western Pacific oscillator, equatorial easterly wind anomalies in the western Pacific, which are produced by western Pacific off-equatorial cold SST and high SLP anomalies, induce an ocean upwelling response that evolves eastward along the equator to provide a negative feedback. In the recharge–discharge oscillator, equatorial wind anomalies in the central Pacific induce the Sverdrup transport that recharges (or discharges) equatorial heat content. It is the recharge–discharge process that leaves an anomalously deep (or shallow) equatorial thermocline that serves as the phase transition for the coupled ocean–atmosphere system. The advective–reflective oscillator assumes that anomalous zonal currents associated with wave reflection at the ocean boundaries and mean zonal current tend to stop growth of El Niño. In nature, all of these mechanisms may be operating.
The 1982–83 and 1997–98 El Niños are two the strongest warm events (with large anomaly amplitudes) on record. Both of these events show western Pacific anomaly patterns in addition to eastern Pacific anomaly patterns (Wang and Weisberg 2000). For example, in the onset and development phases of the 1997–98 El Niño, two off-equatorial anomalous SLP cyclones exhibit in the western Pacific. These off-equatorial low SLP anomalies produce equatorial westerly wind anomalies in the western Pacific. The equatorial westerly wind anomalies in the western Pacific cause the warming in the equatorial central and eastern Pacific. As the 1997–98 El Niño continues toward maturity, SST anomalies in the off-equatorial western Pacific reverse sign from warm to cold. These off-equatorial cold SST anomalies are accompanied by the sign reverse of off-equatorial SLP anomalies from low to high. The off-equatorial high SLP anomalies then initiate equatorial easterly wind anomalies in the western Pacific that force eastward propagating upwelling Kelvin waves and hence affect the anomalies in the equatorial eastern Pacific. Consistent with the results of the unified oscillator model, a combination of western Pacific wind-forced response and wave reflection at the western boundary may have been contributing factors in such a strong event as the 1997–98 El Niño.
In the formulation of the unified oscillator of Eq. (10), we used the dynamics of off-equatorial wind stress curl-induced Rossby waves [also in Jin (1997a)]. This is consistent with observational results of White et al. (1987 and 1989) and Kessler (1990). However, the role of off-equatorial Rossby wave reflection at the western boundary in ENSO has been controversial (Battisti 1989; Graham and White 1991). Battisti (1989) investigated the role of off-equatorial Rossby waves observed in the western Pacific during ENSO. He found that off-equatorial Rossby waves are formed through both wind stress curl and eastern boundary reflection of the equatorial Kelvin wave signal generated in a warm event. His coupled model further suggested that the Rossby wave signals outside of 8° latitude of the equator provide virtually no contribution to the reflected Kelvin wave, thus they probably should not be thought of as the triggering mechanism for an ENSO event. In contrast, Graham and White (1991), using the coupled model of Zebiak and Cane (1987) very similar to that of Battisti (1989), showed that the behavior of the model is greatly altered when effects from poleward of 7° latitude are neglected. They thus concluded that off-equatorial Rossby waves in the western Pacific are important for ENSO. Both of these studies show the existence of off-equatorial Rossby waves, consistent with the western Pacific oscillator. In the western Pacific oscillator, off-equatorial Rossby waves propagate from the east to affect Niño-6 thermocline depth and then SST and SLP over there. The off-equatorial SST and SLP anomalies there change the equatorial wind anomalies in the western Pacific that provide a remote response for the equatorial eastern Pacific. This mechanism does not require the reflection of off-equatorial Rossby waves at the western boundary.
The delay times associated with negative feedbacks of wave propagation are not constant. The ocean–atmosphere coupling gives rise to slow modes and modifies the equatorial wave modes (Hirst 1986; Neelin 1991; Wang and Weisberg 1994, 1996). As shown analytically by Wang and Weisberg, the modifications depend on frequency and air–sea coupling. The primary modifications are in low-frequency bands, with a decrease in phase speeds of Kelvin and Rossby waves. The slow mode and the phase speed decrease of equatorial waves are observed in previous studies (e.g., White and Tai 1992; Chao and Philander 1993). Thus, the ocean–atmosphere coupling changes negative feedbacks associated with wave propagation and reflection. In reality, different negative feedbacks may also interact with one another.
All the conceptual oscillator models for ENSO produce periodic solutions, whereas ENSO variability in nature is known to be irregular. Introduction of stochastic atmospheric forcing of weather noise to an otherwise perfectly periodic oscillatory system can lead to irregular or chaotic oscillations (e.g., Graham and White 1988; Penland and Sardeshmukh 1995; Moore and Kleeman 1999). Interactions between annual and interannual cycles (Jin et al. 1994; Tziperman et al. 1994; Chang et al. 1995; Wang et al. 1999a) can also produce irregular and chaotic oscillations. There may be many reasons for ENSO irregularity, but even for a simple system of linear equations the recognition that nature does not provide a constant parameter medium leads to irregularity. The temporal variations of parameters in nature may also determine the relative role of different ENSO mechanisms where the parameters may be more or less important for each evolving ENSO. For example, the western Pacific may have relatively more influence on strong El Niño events than weak El Niño events because the western Pacific shows strong equatorial wind anomalies for strong El Niño events. In terms of the unified oscillator, temporal variations of the parameters b1 and b2 may determine the relative importance between the delayed oscillator and the western Pacific oscillator.
This work was supported by the NASA (National Aeronautics and Space Administration) Seasonal-to-Interannual Prediction Project (NSIPP), Grant NAG5-8229. I thank R. Weisberg for scientific discussions during the time when I worked at USF. I thank D. Enfield, D. Mayer, and two anonymous reviewers for their comments that helped to improve the manuscript.
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Pleading Cycle Set For Comment On TRS Certification Applications
Federal Communications Commission
News Media Information 202 / 418-0500445 12th St., S.W.
Washington, D.C. 20554
Released: April 16, 2013
PLEADING CYCLE ESTABLISHED FOR COMMENT ON APPLICATIONS FOR
CERTIFICATION FOR THE PROVISION OF TELECOMMUNICATIONS RELAY SERVICE
CG DOCKET NO. 03-123
Comments Due: April 29, 2013
Reply Comments Due: May 13, 2013
certification of their State Telecommunications Relay Service (TRS) program pursuant to Title IV of the
Americans with Disabilities Act (ADA) as codified in the Communications Act, 47 U.S.C. § 225, and the
Commission’s rules, 47 C.F.R. §§ 64.601-605. Current state certifications expire July 25, 2013. A state’s
application for certification, covering the five year period from July 26, 2013 to July 25, 2018, must
demonstrate that its TRS program complies with Section 225 and the Commission’s rules governing the
provision of TRS.1 This notice seeks public comment on the following state applications for certification,
which can be found on the Commission’s Electronic Comment Filing System (ECFS) at
http://apps.fcc.gov/ecfs//. When searching for the state application in the ECFS, please enter docket
number 03-123 in the proceeding number fill-in block, and the state identification number, (i.e., TRS-19-
12) assigned for that specific state application in the bureau identification number fill-in block:
File No: TRS-19-12
File No: TRS-61-12Department of Commerce
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U.S. Virgin Islands
File No: TRS-06-12
State of West Virginia
Pursuant to Sections 1.415 and 1.419 of the Commission’s rules, 47 C.F.R. §§ 1.415 & 1.419, interested
parties may file comments on or before
April 29, 2013, and reply comments on or before
May 13, 2013.
All filings must reference
CG Docket No. 03-123and the relevant state identification number of the state
1 Section 225 states, in pertinent part, that the Commission may approve a state’s application if it determines that the
state’s program makes available TRS “in a manner that meets or exceeds” the Commission’s TRS requirements and
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program.” 47 U.S.C. §§ 225(f)(2)(A) and (B).
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Stuck In Love turns out to be a decent film, a few nice jokes and humourous elements, some cliched but sweet thoughts on romance, love and humanity, and very nice to look at, just a shame it's all so muddled and happy to settle for mediocrity.
[VIDEO ESSAY] A well blended cocktail of familial connections, aspirations, and separations, "Stuck in Love" is a complex romantic comedy that keeps on giving even when you think it has run its course.
Enjoyable and engaging relationship comedy drama enlivened by likeable performances, a strong script and some appealing location work, though it's also a little too pretentious for its own good in places.

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2006 CHRYSLER 300 SRT8 FUSE DIAGRAM
Chrysler 300 (2006 - 2007) – fuse box diagram - Auto Genius
Nov 09, 2017Chrysler 300 (2006 – 2007) – fuse box diagram. Year of production: 2006, 2007. Power Distribution Centers Front Power Distribution Center. A power distribution center is located in the engine compartment. This center contains fuses and relays.
2006 Chrysler 300 Fuse Box Diagram | Fuse Box And Wiring
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Fuses and relays box diagram Chrysler 300
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2006 300C Fuse Types | Chrysler 300C & SRT8 Forums
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The small, two-inch camera attachment clips on the top of the phone and allows health professionals to examine a key area of the interior surface of the eye called the fundus. The fundus includes the central retina, optic disc, macula, fovea and the posterior pole.
|The smartphone camera attachment provides a clear look at the interior surface of the left eye of Barrett Kumke, a 5-year-old from Gibbon, Neb. Kumke was born with a scar on his eye, a condition called ocular toxoplasmosis. He eventually will need surgery.|
Omaha pediatric ophthalmologist, Donny Suh, M.D., has been involved in a research study published in the July edition of the Open Journal of Ophthalmology. The study looked at one of the three similar devices that are in the marketplace.
Dr. Suh is associate professor in the UNMC Department of Ophthalmology and Visual Sciences. He sees patients at Children's Hospital & Medical Center as well as the Truhlsen Eye Institute at UNMC.
Dr. Suh uses the attachment in his practice every day to teach the students and residents. The device costs around $300-$400. In comparison, the existing equipment used by ophthalmologists to examine the optic nerve and retina would be much more expensive, he said, and is not easily portable.
He said the smartphone camera attachment has three key uses:
- As a teaching device for medical students and resident physicians;
- As a tool that referring physicians can use to document eye problems and then forward the image on to ophthalmologists for their expert opinion; and
- As a tool that would allow health professionals on medical missions in foreign countries to take an image of the eye and then forward it back to ophthalmologists for their review.
"It is a great teaching device and can potentially be used in diagnosing a variety of diseases. I think it could revolutionize the way we teach students," Dr. Suh said. "With the ophthalmoscope, I really don't know what the students are seeing. With the smartphone device, students can take pictures and videos of the eye. I know exactly what they are looking at."
Enjoyed hearing more about this at lunch today. Thanks for sharing.
Amazing - what an incredibly powerful tool! Thank you for investigating and sharing what you've found!!

domain: news


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• High gloss formula provides the ultimate shine on all surfaces: metal, carbon fiber, plastic, rubber and vinyl. • Polishes and protects in one easy step • Use on bicycles, fitness equipment, motorcycles, watercraft, ATVs and more. • Slick film helps prevent dirt build-up on frame and parts.
Park's PolyLube is specifically formulated to protect bearing components. Its Polyurea grease has extremely high shear strength to protect bottom brackets, headsets, pedals and hubs. Use it on threads, seatposts, stems and cables, too. It's also safe for fork seals, and repels water.
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Keep your drivetrain quiet while protecting your components with Squirt Dry Lube. This long-lasting wax and water-based lubricant is low maintenance and easy to apply: no degreasing is needed, just squirt it on and ride. Squirt is 100% biodegradable and doesn't contain harmful solvents. Plus, it works in all-conditions, wet or dry, for mountain and road.
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domain: chemistry


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Phil goes riding on the TransPeak service from Derby to Manchester – via some stunning scenery…
I’m loitering around Derby bus station, watching the plethora of TrentBarton’s rainbow of brands bringing people into, and taking them away from, this East Midlands City.
The plan is to ride the TransPeak service across England’s green and pleasant land to the great northern powerhouse of Manchester. I’m struck with irony that TrentBarton’s Red Arrow glorious beasts – high spec brand new coaches that wouldn’t be out of place on a trek across Europe – will whisk their passengers to Nottingham in little more than half an hour to nearby Nottingham, whilst I will spend the next three hours on a service bus to my illustrious destination.
At stand 21, four takers are awaiting the TransPeak. It rolls in, looking rather glamorous in it’s green livery as our driver beckons us on.
TransPeak is operated by High Peak Buses – a joint venture between the aforementioned TrentBarton’s parent Wellglade and CentreBus. The “TP” service is basically hourly from Derby to Buxton, but extends 4 times per day to Manchester.
a single from Derby to Manchester is £8
It’s an impressive welcome. Our friendly driver tells me it’s £8 single for the trip to Manchester, sorts me out quickly and efficiently, and I take my seat on the offside, near the emergency exit (where, for someone 6’7” like me, extra legroom can be a Godsend). My fellow gaggle of passengers choose their spots; a girl with a suitcase and a guy with a pair of the biggest headphones I’ve ever seen. He’s asleep within seconds.
The bus itself is very well-appointed. There’s a wood-laminate effect floor and super-comfortable green/black leather seats. Wifi is available (and it works), as well as USB charging points lurking under the seats in front. There’s no audio/visual announcements though.
We’re off spot on time. I’m constantly impressed at the amount of reversing movements out of the stands at Derby bus station. Drivers must have telepathic skills as you never know what is appearing backwards from behind a stationary vehicle.
Into the gloomy grey skies of a typical Derby January morning. Suitcase girl optimistically tries to put make up on, then thinks better of it as the stop-start traffic isn’t the best environment in which to carry out such a process.
Soon out of the City Centre, we pass through attractive Duffield, then wind our way towards Belper, where a man with a giant fishing rod almost hooks us at speed. Without a flap, we’re soon at what looks like a small bus garage, masquerading as a bus station. This is listed in the timetable as “TrentBarton Bus Garage”. Here, three people join us and we swiftly leave, our driver waving at a TrentBarton bus, whose driver has kindly let us out into the traffic.
We push on, through Ambergate and a sign telling us it’s 53 miles to Manchester. Our man in headphones isn’t remotely interested in the view – he’s pumping up the volume with his huge headphones and most definitely out for the count.
The rain has begun to fall as we follow the path of the River Derwent immediately to our left, and soon we’re into the tourist magnet of Matlock. I make a mental note to return here in more clement weather. Not many tourists today for this pretty part of Derbyshire.
At Matlock Rail Station, there is a small bus station. It’s also very quiet here, and as we’re a few minutes early, our driver awaits time. The only other vehicle here is one bearing the name Hulleys of Baslow – a firm that has always fascinated me as I had a book about the firm as a child, and they were one of only a handful of companies that bought Midland Red buses second-hand, including some S6 models in the 1960s. I’ve never actually caught a Hulleys service, so more mental notes are recorded to return here and put that right!
Our TransPeak service is beginning to fill up and we continue northwards, weaving our way through ancient highways, past stone-clad houses, wintery fields and the obligatory garden centre. TrentBarton’s bright yellow “theSixes” buses are in front of us, and passing in the opposite direction.
The “TP” TransPeak service covers some beautiful scenery
Then we’re out into the real rugged landscape of the Peak District, now following the River Wye on our right. Next up is the delightful town of Bakewell. Our bus stops to collect more travellers opposite the “Bakewell Deli”, with “puddings and tarts” for sale in the window. I momentarily consider asking our driver to wait as I submit to my sweet tooth, but think of my bathroom scales and ever-expanding waistline before thinking better of it. But if I return to ride some Hulleys services in the summer, I can’t guarantee I’ll have the same willpower.
Soon we take a sharp right off the beaten track and our Enviro 200 makes easy meat of the incline into the ridiculously pretty Ashford-in-the-Water, which could easily appear in some period drama. A woman in an ornate stone bus shelter shakes her head to indicate she doesn’t want our TransPeak, but our driver stops anyway, opens the doors and bids her a good morning. It’s all very civilized.
The wind is picking up. It’s the remnants of “Storm Jonas”, which has brought chaos to parts of America. It’s also brought chaos to our next passenger’s hair as she emerges from another shelter that hasn’t done too much sheltering to flag us down. Our driver offers scant commiserations and hands her her concessionary pass ticket and awaits her to be seated. The topic of conversation between her and fellow travellers is now, of course, the weather. I’m tempted to join in, given my plan to take views of the scenery from the bus window has been thwarted by the wind and rain now lashing our vehicle.
But the journey is at least “atmospheric” as we meander past barns and ancient stone walls before our rural scene gives way to civilisation in the form of Buxton.
Buxton is larger than I thought. It’s bustling, despite the weather. Here we exchange most of our travellers for new ones, sporting the morning’s shopping. Most of them seem like regulars and the topic of the weather again echoes around our bus.
Next, we’re exchanging our driver for a new lady model. We’re at Dove Holes, home to High Peak Buses and base of our TransPeak bus. Pleasantries are exchanged and mutual waving takes place between our drivers and the occupant of the driving seat of a “Skyline 199” who has arrived from the opposite direction – Manchester Airport. I decide to take in some music, and Shirley Bassey wails “Goldfinger” from deep inside my mp3 player.
On towards the big City we head, passing pubs with delightful names such as “Dandy Cock” and “Soldier Dick” a the stunning scenery gradually gives way to suburbia in the form of a sign for Stockport and the first glimpse of a Greater Manchester bus stop.
Soon we hit Hazel Grove, where Stagecoach have instigated a Park & Ride using their super-frequent 192 service to the City Centre. From now on, the rest of the journey is punctuated almost consistently by Stagecoach 192s and I wonder just what the peak vehicle requirement might be for this service!
Through Stockport itself we pass, as the giant railway viaduct looks down on the bus station below. The calm serenity of the highways and byways of the Peak District is replaced brutally by the suburban throb of huge amounts of traffic. We pass the McVities factory on the left and the O2 Apollo on the right. The TransPeak is now a limited stop service and we don’t have any takers or leavers as we head inbound towards the metropolis.
And, three minutes early, we pull into Chorlton Street Coach Station in the centre of Manchester, where we rub shoulders with National Express coaches heading off in all directions across the country. Our driver thanks us all as we leave, and I almost expect a hat to have gone around – the TransPeak seems more like a day trip than a bus service. Our Enviro 200 has performed excellently, both in the windswept country lanes and demanding City Centre enviromnments.
Outside the rain has stopped but the wind buffets the great northern powerhouse. I go in search of barm cakes whilst, just 25 minutes later, our TransPeak leaves for another run across the beautiful Peak District back to Derby. This truly is a Great British Bus Journey.
The TransPeak bus emerges from Manchester’s Chorlton Street Coach Station into the gloom of a dull January day on it’s 3 hour run back to Derby
For more information on TransPeak, visit the High Peak Buses website at: High Peak Buses TransPeak website
Live Twitter information at: High Peak Buses Twitter
Historical TransPeak (with information from Mark Fitchew)
The TransPeak evolved from the 252 Nottingham – Manchester service, started in 1985, jointly operated by Trent & Ribble. Ribble’s share soon disappeared at deregulation barely a year later, but Trent kept at it, converting it to “TransPeak” in the early 1990s.
The route number 252 was chosen because it was similar to National Express’ 952, which ran from Nottingham to Manchester (then on to Blackpool) via Mansfield, which originated from a joint Trent / North Western express service. The stretch of the TP from Derby – Matlock was originally Trent / North Western’s 4 service.
The original Derby-Manchester service was the Trent / North Western X1 via Ashbourne. This became the 201 in National Bus Company days (though Beresford competed as X1 in the early 80s with ex Green Line RP AEC Reliances) becoming a tendered service at deregulation, initially operated by Shearings and latter GMS (with Charterline coaches) before its demise.
Mark Fitchew drives buses for National Express West Midlands. You can read more from Mark’s blog here

domain: travel


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MineCraft TNT Party
Your kids will love our new TNT Minecraft Party Range. Packed with loads of great party tableware and decorations to create an awesome Minecraft Inspired Party Room.
From Happy Birthday Banners, Dynamite Party cups, plates and Swirl Decorations to hang from your party room - we have everything you need to build your own Minecraft adventure.
Mix it with our Lime Green, Gold and Red party supplies and decorations to create an awesome TNT party room.
Fun colours to mix and match with your TNT party:
- Lime Green

domain: design


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Have you written a book? Are you ready to share it with the community? The Northbrook Public Library is accepting author requests for the first annual Up & Coming Author event, which will be held on Saturday, August 13.
Take your mark…get set…GO READ!
Call for Film Submissions: Northbrook Youth Film Festival (Grades 7-12)
Prepare to experience a totally radical flashback: in April, the Northbrook Public Library will celebrate the iconic 1980s with a month of ‘80s-themed events.
In 2015, April officially became Autism Awareness Month in Northbrook, marked by the Village’s official proclamation and the Northbrook Public Library’s first
On a snowy March afternoon, Northbrook resident Phyllis Kosner laid out her latest crochet project at the Northbrook
The Northbrook Public Library is partnering with Game On! Sports 4 Girls to present a new month long reading program for girls: Game On!
Libraries are often known for their annual Summer and Winter Reading Clubs, and the Northbrook Public Library is no exception.

domain: library


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Illegal immigrant jailed after sexually assaulting two women in sea at packed UK beach.
Kuku Machhal groped two women in the sea in separate attacks at Bournemouth beach last year. For this, he was sentenced to 18 months’ in jail.
He has also been placed on the sex offender’s register for five years.
Both attacks took place at the beach on July 23, 2021.
His friends are said to have cheered and laughed about what had happened.
Judge David Melville QC, on the other hand, found no reason for joviality.
He described Machhal’s actions as “intimidating” and “degrading”.
He added that both victims were vulnerable because they were in the water.
Machhal attempted to use this fact to his defence.
Judith Constable of the prosecution, said Machhal accepted that he touched the first victim but he claimed there had been a “strong current which brushed him into her”.
He also denied doing anything wrong to the second victim.
But after initially denying both allegations, he changed his plea to guilty.
Machhal is 31 years old.
He arrived illegally in the UK from India in 2015.
Brexit victory! Thousands of farmers cash in on 'golden opportunity' [REVEAL]
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Brexit LIVE: Truss holds talks with Coveney TODAY [LIVE]
Both of his victims reported the attacks to the authorities and Machhal was stopped from leaving the beach by security staff until the police arrived, the court heard.
Lesley Manley of the defence claimed Machhal was sorry for what he had done.
She said: “On that day, Mr Machhal did not go there with any premeditated intention to do harm but obviously his behaviour was not what one would expect.
“Nothing like this has happened before and it is extremely unlikely, I submit, that this behaviour would ever be repeated.”
But Judge Melville took another view.
He told the court: “There was a degree of planning and you did of course have your friends with you as well.
“I do no accept that you are remorseful. When interviewed you accepted no personal responsibility at all.”
Machhal, in the UK illegally, faces deportation, according to his defence.


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Melanie Deal is an Evanston artist who is the latest to be featured in our ongoing exhibition series Local Art @ EPL. Inspired by her fascination with grids, tessellations, and repeated shapes, Deal’s striking paper collage and mixed media works “reflect both the humdrum and the humor of everyday living” and are “influenced by a lifelong love of comic books, paper dolls, gumball-machine trinkets, board games, television, literature, and music.” You can catch her exhibit Life on the Grid through the end of July on the 2nd floor of EPL’s Main Library, and you can also find more of Deal’s work by visiting her website. We recently spoke with her via email about her ingrained love of grids, the meaning of her art, and the burgeoning Evanston art scene.
Evanston Public Library: Can you tell us a little about your background as an artist? How did you get started in art? What are some of the comic books, board games, TV shows, and songs that most influenced you?
Melanie Deal: I was that child in the corner, always drawing. My mother carried blank sheets of paper in her purse so I could draw during church, for example. I made paper dolls, picture books, and comics. Because I loved to read comic books—from Little Lulu to Archie to Marvel Comics—I made my own comic books, with my own teen and superhero characters. As I got older, I made comic strips starring my friends and eventually moved into collage and mixed media.
EPL: Do you see your collage and mixed media works as fitting in with any particular artistic movements or styles? What is it about grids, tessellations, and repeated shapes that so intrigues you?
MD: I didn’t study art—I have degrees in English literature instead—so I’m not sure if my work fits into any particular style. Because I like to use repetition of images, some people have mentioned Andy Warhol as an influence. But really, I just do my own thing. Where did my attraction for grids come from? I grew up in Indiana, which was laid out in 6×6-mile townships in the late 1700s as part of the Northwest Ordinance. Everything is square and easy to navigate there, so maybe that’s ingrained in me. I like repetition because I find it funny—a mildly amusing image seems exponentially funnier and more absurd to me when multiplied.
EPL: Can you take us through your creative process for one of the collages you’re showing this month?
MD: “Creative process” sounds pretty lofty for what I do. I usually start with an idea, which may be as simple as a pattern or set of colors I’d like to work with. I plot it out on graph paper to figure out what size it will be. I gather my materials, such as paper, printouts, book pages, and cartoon word balloons. For “Dusty,” one of the artworks in my library show, I added doll-sized combs, brushes, mirrors, and hair rollers for fun. Sometimes I draw some of the paper pieces by hand. I cut out the pieces and glue them to gatorboard (like foam core, but sturdier), often in layers. It can be a painstakingly slow process, but I have no real reason to rush. And besides, I’m having fun!
EPL: What are your future goals and plans as an artist?
MD: I’m not sure that I have any specific goals as an artist, other than to keep working at it and showing my work when the opportunity presents itself. Although I’m not good at talking about my art, I do like hearing people’s thoughts as they view it. To me, an artwork “means” only what the viewer gets out of it—and each person brings his or her own experiences and perceptions to bear. Sometimes I’m surprised by what people find in my artworks—and that adds to the fun.
EPL: How do you find Evanston and the Chicagoland area as a place to work and exhibit as an artist? What inspires you as an artist about the community where you live?
MD: I used to feel I had to exhibit nationally to build up my resume, but my work is difficult to pack and ship—and that can be very expensive. So now I stick to the Chicagoland area. My favorite venue in Chicago is Woman Made Gallery, where I had my first solo show. Lately, Evanston has become a much richer source of venues than it was in the past, at least in my opinion. There used to be the Evanston Art Center and not much else. Now I always have work on display at Creative Coworking, which has been a real boon to local artists. The Evanston Made show at the EAC is a good opportunity. Besides the library, I’ve also shown work locally at Artruck, Gillock Gallery, As You Like It, Noyes Cultural Center, Gallery 4502, Blick, the Evanston Art Walk, Art Under Glass, and my workplace, Houghton Mifflin Harcourt.
Interview by Russell J.


DAYTON — First, the Ku Klux Klan came to town. Two days later, tornadoes destroyed hundreds of homes and businesses and obliterated entire neighborhoods in and around the western Ohio city of Dayton.
Then this past weekend, a gunman stormed onto a crowded sidewalk in the entertainment district — an area of town typically swarming with revelers who stay until the bars close in the early morning — and fired at least 41 shots into the crowd, killing nine people before he was shot dead by the authorities.
"Something just keeps happening," said Amanda Hensler, an owner of a store, Heart Mercantile, that is across the street from where the massacre took place.
The day after the mass shooting — the second within a 13-hour period in America — residents flocked to Hensler’s store to buy T-shirts that read "Dayton Strong," which has become something of a motto for this grieving, shocked city. The customers knew that the store would have them in stock because they had been printed three months earlier, after the catastrophic tornado outbreak.
Indeed, Dayton has been through a brutal six-month stretch, even before the Klan held a rally at the city’s downtown Courthouse Square. Since the beginning of February, the city has also endured a large infrastructure failure and federal indictments at City Hall.
Seeing the city through all this has been Mayor Nan Whaley, 43, a blunt and outspoken Democrat on her second term who is believed to have political ambitions beyond Dayton — a city with about 140,000 residents who have endured more trauma this year than many larger cities experience in a decade.
Since Sunday morning, when she first appeared before a throng of reporters, Whaley has found herself in the biggest moment of her political life — and at the worst moment of her city’s modern history. She has been a whirlwind presence across the city, too, talking to victims’ families, briefing reporters and working with the state’s Republican governor to form bipartisan alliances on gun policy.
"She’s going to be governor one day," said Sen. Sherrod Brown, D-Ohio. Brown was not speaking of Whaley’s presence solely over the past few days, but over the whole, bad year.
When Whaley was elected to the city commission at age 29, Dayton, like much of the industrial Midwest, was struggling to recover from a prolonged decline.
But during her nearly six years as mayor, Whaley has presided over a downtown revival, helping redeveloping old buildings and bringing in new people.
And during this time, Whaley has steadily built a larger profile for herself, taking on a leadership role in a national mayors’ organization, speaking openly about the toll of the opioid crisis on the state and briefly seeking the Democratic nomination for governor.


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The words were printed using my computer and printer.
I went to the bank the day the challenge was posted and one of the bank customers had folded a dollar into the shirt. That gave me the idea for this card. The teller said the customer folded pants too.
Hint when you fold the dollar using the instructions in the challenge, fold the bottom up a quarter of the way up or so to give you right length otherwise it is too long at the original length.
The sentiment on the inside of the card were made using my computer and printer.
Date: Tuesday, June 5, 2007 GMT Views: 886

domain: finance


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It is in the United States' best interest to move forward on producing energy domestically, and rolling back Obama-era regulations on the environment and will be done in the "right" way through President Donald Trump's executive order on Tuesday, according to Department of the Interior Secretary Ryan Zinke.
"It's in our best interest to move on energy," Zinke told MSNBC's "Morning Joe" program morning, before the executive order was to be signed. "Producing energy domestically and reasonable regulation is far better than watching it being produced overseas with no regulation."
Zinke said there have been catastrophes in many countries where energy is produced over the years, and energy independence will make the United States stronger overseas.
"Look at Russia," he said. "Russia is in the news every day. How do you combat Russia? Economically. We export liquid natural gas to Eastern Europe, replace a lot of what they're providing to Eastern Europe. Iran, the same thing. If we want to put pressure on Iran economically, we do that by supplanting their exports in crude. And we have to do that by our energy independence as well as infrastructure."
Trump's plan to roll back Obama's regulations has come under fire from critics who say it could be harmful to the environment, but it's better to produce energy in the United States, said Zinke.
He pointed to Congress pointing to the methane rule, passed earlier this year as part of a Congressional Review Act against the Bureau of Management's rules against methane venting and flaring.
"Everyone should realize my position on methane is that it's a waste to vent methane, but we need to have the injection systems in place," said Zinke. "But if you don't have a pipeline, you can't build collection systems and you end up isolating assets. We, as a country, all the above energy policy is prudent. We can do it right, hold industry accountable. But also jobs matter and there's a social cost of not having jobs in this country."
Coal also remains under discussion, but there are other technologies, such as in battery storage, "which could supplant coal in the future."
Coal is under a great deal of pressure, said Zinke, and he believes the market will dictate its future.
"I don't think the government should be in the business of picking winners and losers," said Zinke, but in having cleaner, more efficient energy.
"Look at our grid structure," said Zinke. "We need to work on the infrastructure. I'm a huge infrastructure guy. At the end of the day, investing in infrastructure now will be good for this country. [So is] investing in technology, investing in research so we can make our energy portfolio cleaner over time is the right and prudent path."
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